1 10 12 https://theses.otagogeology.org.nz/files/original/c84fc9b84cf1cceb3b8c46f847e44501.pdf 45d4adb33c4874c4dc59af04256baf3d Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Title A name given to the resource Geology theses OU Geology thesis Thesis or dissertation completed by University of Otago Geology students Location WKT (WGS84) The location stored in WKT (WGS84) format POLYGON ((169.285327900529865 -46.074607818028326,169.292435549858567 -46.070671287935895,169.294341691818033 -46.067756312621569,169.305953117679024 -46.060392818481759,169.327564445005692 -46.056922574799692,169.346191534901862 -46.046803619578739,169.355349798486742 -46.037570414866785,169.371986992279972 -46.03155131644894,169.388078187088155 -46.033847768151773,169.397735171380049 -46.043083559745654,169.401853368040406 -46.071791361338022,169.389499829812053 -46.247629925799053,169.277877358020419 -46.223207773502679,169.285327900529865 -46.074607818028326)) Author last name Last name of the Author Bishop Project type Is it an MSc, PhD, BSc(Hons) or PGDipSci? MSc Abstract The Abstract for this thesis A map and description of the geology of 73 square miles of the Clinton District is presented. The area is underlain by sedimentary rocks of Paleozoic and Mesozoic age with a small area of Tertiary sediments occurring in the northern part of the district. The oldest rocks are those of the Tuapeka Group, mainly indurated greywackes of the prehnite-pumpellyite metagretwacke facies. The structure is not clear but equal area projections reveal fold axes trending north-north-east and plunging at 45* in this direction. The younger Paleozoic rocks have been divided into three groups. the oldest, Waipahi, is probably similar in age and content to the Waipahi Group established by Wood (1956) in the adjacent Gore Subdivision. The Arthurton Group corresponds to the lower part of Wood's Arthurton Group, and a new unit, the Popotunoa Group, is established for rocks probably equivalent to the upper part of the original Arthurton Group. Fossils were found in rocks of the Arthurton Group and included the pelecypod Atomofesma, the brachiopod Lissochonetes, and several gastropods. A new brachiopod, Martinia clintonensis, is described. Most of the species recorded formed part of a shallow water biocoenosis which was exterminated by an influx of volcanic ash. The three groups comprise a marginal eugeosynclinal sequence of volcanic greywackes and sandstones, shales, tuffs, and conglomerates and, in part, belong to the heulandite and laumontite zones of the zeolite mineral facies. The structure and stratigraphic relationships of these groups us not absolutely clear and several possible interpretations are presented. A possibility exists that some of the rocks mapped as belonging to the Waipahi Group are actually younger than the Arthurton and Popotunoa Groups. The rocks are thrown into a series of overturned folds trending north-west south-east and are the oldest rocks of the overturned north-eastern limb of the Southland Syncline. Several steeply plunging minor folds were also recorded, possibly aligned along a north-north-east trending zone. Available evidence suggests that these may be older than those trending north-west south-east. The oldest Mesozoic rocks in the district have been placed in a new group, the Kuriwao Gorge Group, which is approximately equivalent to the Wairuna Peak Beds of Wood (1956). Two formations are recognised, the Kuriwao (lower) and Waiwera (upper) Formations. From rocks near the base of the Waiwera Formation specimens of a new species of Conchostracan were collected and these are described with four more from Etalian strata at Kaka Point. Preliminary work indicates that they may be useful index fossils in the older Triassic rocks of Southland. The Kaihikuan Stage conformably overlies the Waiwera Formation but is very thin, and absent at some localities. It in turn is overlain by the Oretian Stage which forms the southern boundary of the district. The Triassic rocks are conglomerates, volcanic greywackes and sandstones, and tuffs. They fall into the heulandite zone of the zeolite facies. They dip steeply, being sometimes overturned along the northern limb of the Southland Syncline. At Waiwera Gorge they are involved in a subsidiary anticline plunging south-east at approximately 25*. Overall, the Paleozoic and Mesozoic rocks, with the exception of the Tuapeka Group, belong to the volcanic arenite suite, the nomenclature of which is herein defined. The amount of pyroclastic material supplied to the developing geosynclines progressively increased with the passage of time. Freshwater or estuarine coal measures, equivalent to the Gore Lignite Measures (Wood, 1956) and possibly Bortonian-Knintan age overlie rocks of the Tuapeka Group near the Pomahake River. Kaolinitic clays overlie and underlie a seam of low grade lignite, which at one locality is on fire. A description of the mineralogy of a resultant fused sediment is presented which suggests that temperatures in excess of 1500*C were attained for a short time. Tertiary and later deformation has been mainly restricted to gentle warping about north-north-east and north-west axes and largely controls the present topography and drainage pattern. Reverse and normal faulting along the Murihiku escarpment probably occurred during the early Tertiary and resulted in the uplifted Triassic block and possibly in other smaller uplifted blocks in the Paleozoic rocks. Finally a short discussion of the economic geology of the area is presented. Department The department where the student is studying primarily. Geology Named locality Named locality describing the field area location. Clinton Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Identifier An unambiguous reference to the resource within a given context 1962Bishop Creator An entity primarily responsible for making the resource Bishop, David Graham. Date A point or period of time associated with an event in the lifecycle of the resource 1962 Title A name given to the resource Geology of the Clinton district Subject The topic of the resource Map Mesozoic Paleontology Paleozoic Sedimentology Arthurton Group conchostracan https://theses.otagogeology.org.nz/files/original/c517170fc904013b9d1b4f25c145692f.pdf 50b4bac97033698dabce16e805f28ba0 Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Title A name given to the resource Geology theses OU Geology thesis Thesis or dissertation completed by University of Otago Geology students Location WKT (WGS84) The location stored in WKT (WGS84) format POLYGON ((167.886525371422522 -45.9081087858739,167.890849285907194 -45.872220089952989,167.955507436588903 -45.875457533180082,167.952786264137785 -45.911062301426306,167.886525371422522 -45.9081087858739)) Author last name Last name of the Author Kennedy Project type Is it an MSc, PhD, BSc(Hons) or PGDipSci? BSc(Hons) Advisers Who supervised/advised this student Landis, C.A. Campbell, J.D. Kawachi, Y. Abstract The Abstract for this thesis Approximately 17,200 ft. of Permian strata, exposed on the south-east margin of the Takitimu Mountains Southland, New Zealand, are chiefly andesitic and basaltic lavas and diorite silts, as well as clastic and sedimentary rocks whose constituent particles were derived from Permian pyroclastic eruptions of augite (and hornblende) andesites. These rocks were steeply tilted and eroded before the deposition of Triassic volcanogenic sediments which now rest unconformably on the Permian strata. During diagenesis volcanic glass has crystallized to heulandite and analcime, and associated minerals are chlorite, celadonite and prehnite. Plagioclase has altered to albite and one or more hydrous Ca-bearing minerals, including prehnite. Albitization is incomplete on every scale. Laumontite is only found in veins, and stilbite is common in cavities of volcanic rook. Gravimetric determination of the amount of silica in two of the Permian basalts gave values of 48.87 and 48.16%.Average K2O, Na2O and K2O:Na2O values for Permian Volcanics are respectively 1.091 3.23 and 0.29, which coincide with volcanic belt No.1 of Challis (1968). The discovery of Mellarium in a partly calcified conglomerate establishes the presence of a new Etalian locality near Wilanda Downs. A new Formation in the Productus Creek Group (Mt. Wilanda Limestone) is defined. Department The department where the student is studying primarily. Geology Named locality Named locality describing the field area location. Takitimu Mountains Thesis description Number of pages, maps, CDs, etc. 65 Leaves. Photos, map (folded in pocket); 30 cm. Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Identifier An unambiguous reference to the resource within a given context 1969Kennedy Creator An entity primarily responsible for making the resource Kennedy, TJ Date A point or period of time associated with an event in the lifecycle of the resource 1969 Title A name given to the resource Geology of the South-East Margin of the Takitimu Mountains, Southland, New Zealand. Subject The topic of the resource Map Igneous petrology Sedimentary petrology Paleozoic Murihiku Supergroup Permian https://theses.otagogeology.org.nz/files/original/27da403f1bf00a74c1363b036e6ebf7c.pdf dd5020b45eac5d20a7dc1ec874da8f5a Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Title A name given to the resource Geology theses OU Geology thesis Thesis or dissertation completed by University of Otago Geology students Location WKT (WGS84) The location stored in WKT (WGS84) format MULTIPOLYGON (((168.106821534000119 -45.272236923999948,168.099704544000048 -45.353349782999935,168.098304417000122 -45.36926046699994,168.097710299000028 -45.376001018999951,168.094169331000103 -45.416242452999938,168.094005365000044 -45.418097089999932,168.080946251000114 -45.41752798199996,168.07928537500004 -45.417453279999954,168.068276793000109 -45.416969369999947,168.067530676000075 -45.416937754999921,168.053235758000028 -45.416304059999952,168.018608661000059 -45.414768465999941,168.024241846000137 -45.350117864999952,168.025120023000113 -45.340026805999969,168.027040405000093 -45.317962990999938,168.030894646000121 -45.273623970999942,168.031287591000023 -45.26908355199999,168.021082243000023 -45.268650829999949,167.981985178000087 -45.266994317999945,167.977377146000123 -45.266799509999942,167.978071127000021 -45.258544162999961,167.979273678000027 -45.244274839999953,167.988156429000043 -45.138544670999963,167.995097274000074 -45.060250461999942,167.998419775000116 -45.022717446999927,168.006043699000088 -44.93636989,168.061910163000135 -44.938632691999928,168.067194752000091 -44.938844997999986,168.119527070000117 -44.940937253999941,168.144731618000037 -44.941936129999924,168.134112943000105 -45.06617915299995,168.126855400000096 -45.15074882399994,168.126822970000035 -45.151135097999948,168.118964687000016 -45.248286294999943,168.117677135000122 -45.264170287999946,168.117581114000018 -45.265347185999985,168.116986873000116 -45.272660225999978,168.106821534000119 -45.272236923999948)),((168.066082992000048 -44.925179793999973,168.023258259000016 -44.923522089999949,168.023303336000026 -44.922919984999965,168.02398464500007 -44.913789469999976,168.029316868000052 -44.85026077,168.030458310000114 -44.836448450999967,168.033542663000048 -44.799080951999919,168.040105802000113 -44.719395543999944,168.044872859000066 -44.66557522799998,168.057405057000096 -44.522002480999959,168.058014632000095 -44.514983179999945,168.061623832000123 -44.473478419999935,168.062799976000065 -44.473529067999934,168.076689560000091 -44.474108229999956,168.093349374000013 -44.474799718999968,168.156419421000152 -44.477394812999925,168.186345674000137 -44.478613817999971,168.220813070000077 -44.480009544999959,168.241586597000065 -44.480845752999976,168.240462704000066 -44.493761835999962,168.239243782000017 -44.507728659999934,168.237439607000056 -44.528404977999948,168.237335757000125 -44.529608601999925,168.236566619000087 -44.53839730199995,168.233609276000067 -44.572286069999961,168.213868873000052 -44.605283656999966,168.210095314000114 -44.611589943999959,168.206881912000114 -44.65091741,168.205134337000118 -44.672281321999947,168.203639210000148 -44.690545733999954,168.201628171000038 -44.715094355999952,168.191110734000091 -44.843123558999935,168.188193894000079 -44.878524221999967,168.183974053000071 -44.929659743999927,168.145010263000046 -44.92819112199993,168.120627166000077 -44.927267347999916,168.074051681000014 -44.925488453999954,168.066082992000048 -44.925179793999973)),((168.256676420000076 -44.259981604999943,168.246447166000053 -44.259557022999942,168.248368448000065 -44.224251490999961,168.249452667000043 -44.204306611999982,168.249627067000119 -44.201096985999975,168.283657356000049 -44.201512615999945,168.285626165000053 -44.201536346999944,168.296592034000042 -44.201667890999943,168.356834553000112 -44.202371472999971,168.387082412000041 -44.202712568999971,168.434902555000122 -44.203235239999955,168.433723120000082 -44.227276540999974,168.433401976000027 -44.233818777999936,168.432323633000124 -44.255774295999956,168.431766815000088 -44.267104050999926,168.413641506000118 -44.266379434999969,168.407930165000039 -44.266150497999945,168.370108459000107 -44.264627098999938,168.354848383000103 -44.264008830999941,168.28088285700008 -44.260982603999935,168.256676420000076 -44.259981604999943))) Author last name Last name of the Author Landis Project type Is it an MSc, PhD, BSc(Hons) or PGDipSci? PhD Advisers Who supervised/advised this student Coombs, D.S. Abstract The Abstract for this thesis Stratigraphy and lithology of Upper Permian and overlying Triassic rocks of the Key Summit-Nelson Regional Syncline are described. In general, these descriptions verify earlier stratigraphic observations by Wellman, Grindley, Waterhouse, and others. However, many new data are presented and several stratigraphic refinements and alterations are proposed. It is proposed that the base of the Bryneira Group be extended downward to include a varied suite (ca 150 m thick) of conglomerates, red and green breccias, greenish volcanic sandstones, black siltstones, impure limestones, etc, which underlie the Howden limestone and overlie the highest volcanic rocks of the Humboldt Group. The name Upukerora Formation is proposed for these rocks. Lithologically similar rocks (e.g. upper part of the Glennie Formation) occur at the same stratigraphic horizon in the east limb of the Nelson Regional Syncline. Following deposition of the Upukerora Formation, the area of the Key Summit-Nelson Regional Syncline -- a shallow-shelf at that time -- became the site of extensive carbonate sedimentation. The resulting rocks, the Howden and Wooded Peak limestones, consist very largely of comminuted (sand grade) prismatic shell fragments which were derived from the bivalve Atomodesma. Terrigenous debris, largely volcanogenic, comprises a relatively minor part of these rocks. The limestones are thin to absent in the southern part of the Key Summit Regional Syncline and in the northern part of the Nelson Regional Syncline. Thickness in the area between Key Summit and Mt. Barrington varies from 400-1000 m. Newly discovered Howden exposures are recorded from the west limb of the Key Summit Regional Syncline. These rocks resemble closely their east limb correlatives and also correlative strata in the Productus Creek Terrane. Similar Rocks also occur in the Arthurton Fold Belt and the Torlesse Terrane. It is suggested that a great sedimentary blanket (with a few holes) extended well beyond present syncline boundaries. Facies variations and possible shore-line positions are discussed. Limestone sedimentation was succeeded by the deposition of terrigenous sands which now comprise the Annear and Tramway formations. These rocks comprise thin-bedded, calcareous and fossiliferous, sandstones and siltstones. Thickness of Annear-Tramway strata is generally similar to that of Howden-Wooded Peak strata. In addition, regional thickness variations tend to be in sympathy with variations in Howden-Wooded Peak thickness. The depositional environment remained similar to that of the Howden-Wooded Peak beds (a relatively shallow stable shelf), and Atomodesma continued to flourish. The terrigenous sand portion of Annear-Tramway rocks is distinctly more quartzose and less volcanogenic than other Bryneira-Maitai strata. Current-bedding at Mt. Barrington indicates sediment transport from west to east. Petrographically and stratigraphically similar rocks also occur in the Productus Creek and Torlesse terranes. It is suggested that the Annear and Tramway formations may comprise a portion of a relatively quartzofeldspathic sandstone blanket which originally spread across nearly the entire width of the New Zealand Geosyncline. A suite of massive, green, unfossiliferous, volcanogenic sandstones are widespread within both limbs of the regional syncline, and they are commonly quite thick -- 150-1200 m. They are especially well-developed in the vicinity of the Key Summit Ridge, and it is proposed that a new formation, the Key Summit Sandstone, be recognized (previous maps have included both Key Summit and Annear strata within the Howden and Tapara formations). The correlative formation in the Nelson Regional Syncline is the Little Ben Sandstone. Key Summit - Little Ben sediments consist almost entirely of first cycle basaltic and andesitic debris which appears to have been deposited quite rapidly (probably from turbidity currents) in an elongated basin or trench. Formation of this basin appears to have coincided with cessation of deposition of quartzo-feldspathic sediment of the Annear and Tramway formations, and also with the virtual disappearance of Atomodesma from Bryneira-Maitai seas. The axis of the basin of deposition appears to have coincided approximately with the present regional syncline axis. Petrographically and stratigraphically similar rocks of the basal Hawtel Formation occur in the Productus Creek Terrane, however these sands were probably deposited upon a shallow, stable shelf which lay to the west of the Key Summit-Little Ben basin. The coarsely volcanogenic sedimentation of the Key Summit-Little Ben formations ended rather abruptly. Overlying rocks, the Tapara and Greville formations, consist of unfossiliferous, grey, interlaminated sands and muds. Bedding laminae tend to be continuous and undisturbed, and coarser laminae commonly show size grading. Thickness is approximately 1000-1500 m. Fine grain-size of most Tapara-Greville rocks renders evaluation of provenance rather difficult, however, the coarser portion of these rocks contains both volcanic and plutonic debris. Tuffs are present, but uncommon. The tops of the Tapara and Greville formation is defined by an abrupt lithologic change to reddish sediment. These overlying "red beds", approximately 500 m thick, comprise the Winton and Waiua formations. Apart from the presence of hematite, Winton-Waiua rocks bear a very close lithologic and mineralogic resemblance to Tapara-Greville strata. No evidence is recognized for volcanism contemporaneous with Winton-Waiua sedimentation. Textural relations suggest that hematite in these rocks formed during weathering (prior to sedimentation) and also during diagenesis. Sedimentary rocks which may be correlated with Tapara-Greville and Winton - Waiua Strata are not recognized beyond the Key Summit- Nelson Regional Syncline-Arthurton Fold Belt. These sediments probably accumulated in a deep marine trench which was essentially coincident with the Key Summit-Nelson Regional Syncline. The youngest Bryneira-Maitai strata comprise the Countess and Stephens formations. Both units consist predominantly of unfossiliferous green volcanogenic sandstones and associated finer grained rocks; thickness ranges up to 1800 m. Basal Stephens strata, herein named the Gordons Member, are characterized by an abundance of tuffs, conglomerates and limestones. Similar beds, but without limestone also occur at the base of the Countess Formation. Stratigraphic contrasts between Countess and Stephens rocks are described and it is shown that these contrasts may be explained in terms of local geologic structure. Tuffs, limestones and conglomerates of the upper Productus Creek Group (upper Hawtel-Wairaki formations) may be correlated tentatively with Gordons Member. The Countess Formation is overlain unconformably by about 1500 m of conglomerates, tuffs, volcanogenic sandstones and argillites of the Snowdon Formation (new name). These rocks contain Triassic fossils (Etalian Stage). Similar strata appear to overlie the Stephens Formation. A period of latest Permian or early Triassic crustal unrest in inferred. Aspects of regional geology, local stratigraphy and petrography are discussed for all areas known to contain Upper Permian strata. Geology of the Key Summit-Nelson Regional Syncline and parallel adjoining terranes is discussed in detail: ten area maps, each accompanied by a text, are presented. The regional syncline is shown to be nearly isoclinal and to possess remarkable continuity. The eastern synclinal limb is overturned in most areas, and the east-limb contact between Bryneira-Maitai rocks and Lower Permian (Humboldt-Lee River) rocks is characterized by an unconformity. In contrast, the western synclinal limb is consistently "right-way-up", and the contact between Bryneira-Maitai rocks and Lower Permian (Alabaster-Brook Street) rocks is consistently faulted (Hollyford-Waimea Fault). Certain intra-Bryneira-Maitai faults (e,.g. Upukerora and Whangamoa) are shown to be extremely continuous structures. Other areas containing Upper Permian strata are also discussed; these include Productus Creek, Mataura Island, South Canterbury and Parapara Peak. The regional reports also include metamorphic data. Mineral assemblages are tabulated and mineral distribution illustrated with regard to stratigraphic and regional distribution. Positions of mineralogic isograds are reported. Volcanogenic debris in Upper Permian rocks has been very extensively reconstituted under lower grade metamorphic conditions. Mineralogic and petrographic data pertaining to a variety of a authigenic minerals are presented. Some relict detrital minerals are also described. Rock-forming zeolite minerals are restricted to the lowest grade metamorphic rocks studied. In general, data pertaining to these minerals conform with observations of previous workers. It should be noted, however, that some burial metamorphic analcime concentrates possess unusually low silica contents, and also that authigenic analcime, heulandite and laumontite have been recorded from Tertiary rocks from the Hollyford-Waimea Graben and from the Te Anau and Nelson basins. Non-zeolitic Ca-Al-silicate minerals are, petrologically, the most important minerals recorded; they include lawsonite, prehnite, pumpellyite and epidote. Lawsonite, a mineral indicative of relatively high pressures during metamorphism, is especially widespread in Bryneira-Maitai rocks. It occurs in apparent stability with prehnite, pumpellyite and epidote, but not with zeolites. Bryneira-Maitai epidote tends to be iron-rich, and some data suggest that it is of the "high index" variety. Calcite is the prevalent polymorph of CaCO3 in all rocks studied. A few occurrences of aragonite are recorded from the vicinity of ultramafic bodies. Authigenic amphiboles are uncommon. They include tremolite-actinolite, which does not co-exist with lawsonite, and a blue amphibole (probably of the riebeckite-magnesioriebeckite series) which co-exists with lawsonite in at least two occurrences. Metamorphic hornblende occurs in certain Lower Permian mafic volcanic and intrusive rocks. Hornblende also occurs widely, but not abundantly, as a detrital mineral. Clinopyroxene minerals, augite and salite, occur as detrital grains in numerous rocks. Neither jadeite nor any other authigenic pyroxene has been recognized in the Upper Permian rocks studied. Metamorphic diopside occurs in some Lower Permian rocks. Authigenic phyllosilicate minerals include chlorite, sericite, celadonite, stilpnomelane, biotite and montmorillonoid clays. Chlorite is virtually ubiquitous; the optically negative variety is found in rocks of all metamorphic grades, whereas optically positive chlorite is absent from lowest grade rocks but becomes increasingly abundant in rocks of slightly higher metamorphic grade. Sericite, probably phengitic, is also widespread. Celadonite is restricted to the lower grade rocks studied. Several previously unrecorded celadonite-bearing mineral assemblages are listed. Stilpnomelane is restricted to rocks in which reconstitution is well advanced. It co-exists with epidote and with amphiboles, but is very rare or absent in zeolite-, prehnite-, and lawsonite-bearing rocks. Biotite occurs in metamorphosed Upper Permian sediments from Parapara Peak, and in addition it occurs as a detrital mineral in many other rocks. Montmorillonoid clays are restricted to zeolite facies rocks. Microcrystalline Sphene is abundant and widespread. Quartz and albite occur in nearly every mineralogically reconstituted rock. Some rocks contain detrital Ca-plagioclaae and orthoclase which have escaped reconstitution. Oxide and sulfide minerals include authigenic hematite and pyrite, which are both abundant but do not co-exist, minor chalcopyrite and pyrrhotite, and detrital magnetite and chromite. Dispersed carbonaceous material has been concentrated from numerous metamorphic rocks and analysed by X-ray and electron diffraction methods. A classification to describe sub-graphitic material is proposed, and progressive graphitization is discussed. Carbonaceous material in zeolite facies rocks is nearly amorphous; well-crystallized graphite is first recognized in amphibolite facies rocks. Minor occurrences of tourmaline, apatite, garnet, rutile and allanite are also reported. On the basis of these observations, nine metamorphic zones are defined and mapped. They are correlated with recognized mineral facies -- zeolite, prehnite-pumpellyite, lawsonite-albite-chlorite, pumpellyite-actinolite, greenschist, and blueschist. Several subfacies are tentatively recognized. Phase rule considerations and textural relationships are taken to indicate widespread approach to equilibrium, however in many cases the extent of an equilibrium assemblage may be restricted to a microscopic volume or rock. In addition, compositional zoning in certain minerals (e.g. pumpellyite and epidote) implies small-scale disequilibrium. The behaviour and classification of chemical components is discussed. Some evidence suggests that H2O and/or CO2 may not have possessed perfect mobility during metamorphism. A minimum of four and a maximum of seven components (Al2O3 , CaO, FeO, MgO, Fe2O3 , H2), CO2) are considered to be determining components (Korzhinskii terminology). Numerous three- and four-component determining systems are explored chemographically. Comparison of these diagrams provides some clues regarding mineralogic reactions which may define zone boundaries. However, successful identification of metamorphic reactions by this method requires prior correct recognition of the determining chemical components. Successful application of the phase rule also relies on correct recognition of determining components. Bearing in mind this reservation, the writer concludes that phase rule considerations are generally compatible with attainment of equilibrium under di- or multi-variant conditions. Some assemblages suggest possible univariant or invariant conditions, or alternatively disequilibrium. Metamorphic temperatures and pressures constitute the primary controls over distribution of Ca-Al-silicate minerals. The stability fields of most of these minerals overlap. For example, prehnite-pumpellyite assemblage rocks occur interbedded with lawsonite-pumpellyite assemblage rocks in several areas. Possible secondary controls of mineral distribution include chemical composition of the host rock and varying chemical potential of volatile components. These secondary controls are discussed in some detail. The p - t conditions of metamorphism are investigated and a tentative p - t-facies diagram is presented. The formation of lawsonite-albite-chlorite facies mineral assemblages requires an abnormally low thermal gradient, probably less than 15°C/km. The data presented -- stratigraphic, lithologic, structural, and metamorphic -- may be synthesized in a geotectonic history. Upper Permian rocks of South Island, New Zealand accumulated in a rapidly evolving and tectonically complex geosyncline. Numerous paleotectonic (i.e. pre- Rangitata Orogeny) structural elements and geologic terranes can be recognized within this geosynclinal framework: these ancient structures exerted a profound control over geosynclinal sedimentation and also over subsequent tectogenesis. They are recognizable today in such features as the Median Tectonic Line, Hollyford-Waimea Fault, Southland-Kawhia Regional Syncline (i.e. synclinorium), and the Key Summit-Nelson Regional Syncline. Some other major structural features, e.g. Alpine Fault, Livingstone Fault, are not recognized within the paleotectonic framework. Two sedimentary facies belts -- Hokonui and Alpine -- of Permian to Jurassic age, divide the geosyncline into two longitudinal provinces. The facies belts are separated from each other by the Dun Mountain Ultramafic Belt, and it is suggested that this belt may consist partly of sub-geosynclinal basement. Two parallel regional synclines -- Key Summit-Nelson and Southland-Kawhia -- lie within the Hokonui belt. It is emphasized that these structures differ from each other tectonically and chronologically and are nowhere co-linear. Although presently orogenic fold belts, they inherited their structural position and synclinal form from the geosynclinal framework in which they originated. The regional synclines are bordered in part by major faults -- Hollyford-Waimea, Gunn-Eighty Eight -- which are shown to coincide with structural breaks in the geosynclinal basement and also with stratigraphic discontinuities. A model for paleotectonic evolution of the New Zealand Geosyncline is proposed and briefly discussed. Abundant unstable terrigenous and pyroclastic debris as well as deep sedimentary burial rendered Permian rocks mineralogically unstable. Thus zeolite and prehnite-pumpellyite facies burial metamorphism proceeded between Permian and late Jurassic or Cretaceous times. In contrast, structural evidence and K-Ar dates suggest that the formation of lawsonite occurred only during early Cretaceous -- Rangitata -- time. Several important attributes of Upper Permian rocks can be related to width of the Hokonui Facies Belt. These include -- sedimentary facies and stratigraphic thickness, degree of textural reconstitution, mineralogic grade of metamorphism, depth of post-Rangitata erosion, and possibly K-Ar age of slates. Thus highest grade Bryneira-Maitai metasediments lie in the narrow, tightly appressed medial portion of the elongate Key Summit-Nelson Regional Syncline, a position where width of the Hokonui Facies Belt is minimal. Metamorphic grade decreases with increase in Width of the Hokonui Belt. It is proposed that the New Zealand Geosyncline was driven westward into the continental Western Province during Rangitata orogenesis. The Key Summit-Nelson Regional Syncline became uncoupled from the western part of the Hokonui belt and was rapidly dragged deep into the crust, perhaps with the descending limb of a convection cell. Dextral strike-slip movement along the Alpine Fault commenced following the climax of Rangitata orogenesis. Movement probably occurred in spasms, and is still active today. Data presented herein may be regarded as consistent with the hypothesis that the Key Summit and Nelson regional synclines originated as one continuous structure. Displacement along the Alpine Fault severed this structure and separated the two portions by 480 km. Department The department where the student is studying primarily. Geology Named locality Named locality describing the field area location. South Island Thesis description Number of pages, maps, CDs, etc. xxv, 2 vols 1: 316 Pages, 2: 317-624 Pages; 30cm Maps and plate folded in seperated book. Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Identifier An unambiguous reference to the resource within a given context 1969Landis Creator An entity primarily responsible for making the resource Landis, C.A. Date A point or period of time associated with an event in the lifecycle of the resource 1969 Title A name given to the resource Upper Permian rocks of South Island, New Zealand: Lithology, stratigraphy, structure, metamorphism and tectonics. Subject The topic of the resource Map Lithostratigraphy Metamorphic geology Structural geology Tectonics Paleozoic blueschist lawsonite Maitai Group Permian https://theses.otagogeology.org.nz/files/original/48bcea4e8a681b173987a7bb22b0fea9.pdf cf6f2bcca398b74ad580cf2509d15e3c Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Title A name given to the resource Geology theses OU Geology thesis Thesis or dissertation completed by University of Otago Geology students Location WKT (WGS84) The location stored in WKT (WGS84) format POLYGON ((168.119659543000012 -44.939279575999933,168.119527070000117 -44.940937253999948,168.067110221000121 -44.939093817999947,168.061880999000095 -44.938901906999945,168.061910163000107 -44.938632691999942,168.062106685000117 -44.936838016999957,168.062831060000121 -44.930161535999957,168.06608299200002 -44.925179793999973,168.072297500000104 -44.915654509999968,168.085080416000096 -44.896054763999985,168.093130446000032 -44.883703814999933,168.095969731000082 -44.879343938999966,168.124377071000026 -44.880687299999977,168.120627166000077 -44.92726734799993,168.119659543000012 -44.939279575999933)) Author last name Last name of the Author Williams Project type Is it an MSc, PhD, BSc(Hons) or PGDipSci? BSc(Hons) Advisers Who supervised/advised this student Landis, C.A. Abstract The Abstract for this thesis The area round Cascade Creek from the Livingstone Fault to the Te Anau - Milford road has been mapped. Previous work on the Permian sequence in Otago - Southland and Nelson is examined in some detail. Group names applied to the rock formations of the area are; Humboldt, Brook Street and Maitai. Reasons for this nomenclature are given in Appendix 1. A section of the Eglinton Volcanics along Cascade Creek is described, lithologies present include quartz keratophyre, andesite and volcanogenic sediments. An infaulted sliver of Murihiku Supergroup may be represented by one outcrop in the creek. The north end of the southern section of the Livingstone Volcanics occurs one mile south of Cascade Creek. These rocks are briefly described and classified as epidiorites. The Red Mountain Ultramafics consist of sheared serpentinite, blocky serpentinite and tectonic inclusions. X-ray analysis of the sheared serpentinite suggests that all three serpentine polymorphs are present, viz., antigorite, crysotile and lizardite. Two types of tectonic inclusions are recognised, those with dioritic composition, and those metasomatised to rodingite. X-ray analysis of hydrogrossular from five rodingites suggests a low degree of hydration and a formation temperature (630 - 750°C) outside the stability field of serpentine - assumed to be 500°C. Chlorite from inclusion margins is moderately aluminous and rich in magnesium relative to iron. It is not known whether the ultramafics were laid down before the Livingstone Volcanics or subsequently intruded along the Livingstone Fault. The steeply dipping sediments exposed between the Eglinton and Livingstone Volcanics are referred to as the Maitai Group. Volcanic breccias, sandstones and argillites underlying the Howden Limestone, and previously included in the Livingstone Volcanics, are placed in the newly defined Cascade Formation. The type section is situated half a mile south of the triple forks in Cascade Creek. Atomodesma - bearing Annear Sandstone overlies the Howden Limestone and is overlain by the massive, unfossiliferous, well sorted Key Summit Sandstone. Most of the Maitai sediment is volcanically derived. Alkali analyses of the two volcanic suites show a higher K20:Na20 ratio in the Eglinton Volcanics. These results are considered to support Challis' theory that the two belts were genetically distinct. The Key Summit Syncline axis is mapped as a faulted axis along the contact separating the Annear and Key Summit Formations The Livingstone and Hollyford Faults are steeply dipping features approximately one mile apart east of Lake Gunn. The strike directions of two other near vertical faults make an angle of approximately 30° with the Livingstone Fault. They may be part of a conjugate set between the Livingstone and Hollyford faults. Active, or very recent scarps near the top of, and parallel to ridge crests, may be the result of gravitational adjustment in mountains whose slopes have been oversteepened by ice movement. All rocks in the area have undergone regional metamorphism. The Maitai sediments contain lawsonite without prehnite and are classified as lawsonite- albite facies. The Eglinton Volcanics are assigned to the prehnite - pumpellyite facies, and the Livingstone Volcanics to the higher grade pumpellyite-actinolite schist facies. A brief geological history is given. The width of Maitai sediments exposed in Cascade Creek is probably the narrowest anywhere along the marginal syncline, and this area may have the greatest depth of erosion in the syncline. Department The department where the student is studying primarily. Geology Named locality Named locality describing the field area location. Cascade Creek Eglinton Valley Thesis description Number of pages, maps, CDs, etc. vi. 69 p. ill, photos, map (folded in pocket); 27 cm. Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Identifier An unambiguous reference to the resource within a given context 1969Williams Creator An entity primarily responsible for making the resource Williams, JG Date A point or period of time associated with an event in the lifecycle of the resource 1969 Title A name given to the resource The Geology of Cascade Creek, Eglinton Valley. Subject The topic of the resource Map Igneous petrology Sedimentary petrology Paleozoic Atomodesma Cascade Formation serpentinite https://theses.otagogeology.org.nz/files/original/5c7193fbc0ac8d5dbb5d2f218f4636a4.pdf 8abc3013877289673f14779c3e5afb98 Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Title A name given to the resource Geology theses OU Geology thesis Thesis or dissertation completed by University of Otago Geology students Location WKT (WGS84) The location stored in WKT (WGS84) format POLYGON ((168.213425028000074 -46.557384260999989,168.212001495000095 -46.557340453999984,168.20945426500009 -46.557260363999951,168.212945281000088 -46.511373214999935,168.215302350000115 -46.511477197999973,168.217256156000076 -46.511564895999982,168.217821658000048 -46.511592170999968,168.245156483000073 -46.512811048999936,168.260472753000045 -46.513490568999941,168.26775521400009 -46.508856028999958,168.269926317000113 -46.507473603999976,168.271191054000042 -46.506667853999936,168.272183482000059 -46.506035990999976,168.308628771000031 -46.507489328999952,168.308577368000101 -46.508149623999941,168.308518527000047 -46.508899737999975,168.308307507000109 -46.511527188999935,168.306598535000035 -46.532789223999949,168.305831881000017 -46.542315299999984,168.305253205000099 -46.549492364999942,168.304371169000092 -46.560482666999974,168.303505650000034 -46.571230294999957,168.303397110000105 -46.57257767599998,168.27689242200006 -46.571307779999984,168.273326607000058 -46.571134626999928,168.267115691000072 -46.57083363199996,168.267345815000112 -46.568004212999938,168.267852931000107 -46.561784024999952,168.268067209000037 -46.559143208999963,168.26807134000012 -46.559093810999968,168.262250297000037 -46.558911635999948,168.241405655000108 -46.558264106999957,168.228444558000092 -46.557857336999973,168.214060116000041 -46.557405323999944,168.213425028000074 -46.557384260999989)) Author last name Last name of the Author Mossman Project type Is it an MSc, PhD, BSc(Hons) or PGDipSci? PhD Advisers Who supervised/advised this student Coombs, D.S. Abstract The Abstract for this thesis The Greenhills Ultramafic Complex occupies 5 square miles on the north-west part of Bluff Peninsula. It consists of a deformed layered series of ultrabasic rocks of "early late" Permian age intruded into Lower Permian metasediments of the Southland Syncline. The main penetrative planar structures in the complex are primary layering and cleavage; both are inclined. Mesoscopic folds in primary layering are not uncommon. Widespread slumping in the layered series and the emplacement of the complex as a plug of hot rock bounded by a fault and ringed by a "lubricating" marginal gabbro indicate recurring conditions of instability during evolution of the complex. Emplacement of the Greenhills Complex was accompanied by the intrusion of innumerable dykes and by folding and faulting. Two main generations of dykes are recognized: 1) early ultrabasic dykes (in order of decreasing age: dunite, wehrlite and eucrite) are unchilled and preceded emplacement of the marginal gabbro; 2) late dykes (in general order of decreasing age: eucrite, anorthosite, trondhjemite, hornblende-andesite, dolerite, tremolite-picrite, hornblende-plagioclase pegmatite and aplite) are chilled and postdate the marginal gabbro. Emplacement of the Greenhills Complex effected contact metamorphism of country rock spilitic metasediments of the Greenhills Group. These rocks, dominantly volcanic microbreccia with intercalated bands of impure marble, increase from regional prehnite-pumpellyite facies through greenschist facies as seen at Mokomoko Inlet to hornblende-hornfels adjacent the Greenhills Complex. Fossils including the gastropod Peruvispira aff. imbricata Waterhouse and the bivalve Atomodesma aff. marwicki indicate a late Lower Permian age for the middle part of the Greenhills Group. The coral Plerophyllum aff. timorense Gerth occurs in a lower horizon of the Greenhills Group. Bands of marble containing shell fragments and radiolarians are common in the upper part of the section. The layered series of the Greenhills Ultramfic Complex is stratigraphically divisible into: 1) an upper eucritic portion dominated by a 2000 ft thick Eucrite Zone which includes a 50 ft thick allivalite unit; 2) a lower ultramafic portion comprised essentially of a 500 ft thick Wehrlite Zone (which includes near its base a poikilitic peridotite unit less than lOO ft thick) and a basal Dunite Zone exceeding 2000 ft in thickness. A Transition Zone of feldspathic wehrlite occurs between the upper and lower portions of the complex and with the poikilitic peridotite unit is an important marker horizon. The layered series shows well developed accumulate structures and textures resembling cumulates in classic stratiform intrusions. Cryptic layering is shown by the range in composition of the essential primary minerals. These minerals in order of separation from the Greenhills magma are: olivine (Fo90-65 ), clinopyroxene (Ca41Mg54Fe5 to Ca44Mg47Fe9) and plagioclase (An92-88). Other primary minerals present in minor quantities include orthopyroxene (avg. En81), brown hornblende and chromite (Mg48) (Cr60Al22). Optical and X-ray studies of the plagioclases suggest a discontinuity in the unit cell geometry between An90.5 and An93.0; this break probably represents the boundary between transitional and primitive anorthite structures. Single crystal X-ray study of augite lamellae exsolved on (lOO) of orthopyroxene shows that the c and b-crystallographic directions of orthopyroxene host and included lamellae are coincident. The unit cell dimensions of the lamellae as determined after least squares refinement are: aA9.79, bA8.90. cA5.29 all + 0.04 AB106*14' +1', V 442.62 + 0.5 A3. The Greenhills Ultramafic Complex is adequately explained by crystal settling during fractional crystallization of a basaltic magma. This magma is believed to have had affinities transitional between alkaline and tholeiitic magma types. Differentiation took place in a hydrous open system connected with the surface of the earth. OURArchive handle The handle from the Otago University Research Archive (OURArchive) <a href="http://hdl.handle.net/10523/5619">http://hdl.handle.net/10523/5619</a> OURArchvive access level Open Access Department The department where the student is studying primarily. Geology Named locality Named locality describing the field area location. Bluff Greenhills Thesis description Number of pages, maps, CDs, etc. xix, 261 p. : illus., maps (2 fold. in pocket), tables ; 26 1/2 cm. Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Identifier An unambiguous reference to the resource within a given context 1970Mossman Creator An entity primarily responsible for making the resource Mossman, David John. Date A point or period of time associated with an event in the lifecycle of the resource 1970 Title A name given to the resource Geology of the Greenhills ultramafic complex, Bluff peninsula, Southland, New Zealand Subject The topic of the resource Igneous petrology Mineralogy Paleozoic Greenhills Ultramafic Complex layered intrusion Permian ultramafic rocks https://theses.otagogeology.org.nz/files/original/1b0f15b4047e908b339cb20c2c085a22.pdf c6d7478eda35842b5ac76c2240d3de2c Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Title A name given to the resource Geology theses OU Geology thesis Thesis or dissertation completed by University of Otago Geology students Location WKT (WGS84) The location stored in WKT (WGS84) format POLYGON ((167.878369194000015 -46.370050387999981,167.879808100000105 -46.353737961999968,167.879926584000032 -46.352390923999963,167.883119343000089 -46.316101634999939,167.93896656600009 -46.318647471999952,167.97454575200004 -46.320251739999946,168.019321430000105 -46.32225531499995,168.023377735000054 -46.322435170999938,168.051642607000076 -46.32368921799997,168.05150263400003 -46.325630246999935,168.050284278000049 -46.342731661999949,168.04613921300006 -46.40074345599993,167.909204655000053 -46.395211335999932,167.894838918000119 -46.394619168999952,167.876271165000048 -46.393852232999961,167.876658414000076 -46.389465469999948,167.878182414000094 -46.372187733999965,167.878369194000015 -46.370050387999981)) Author last name Last name of the Author MacFarlane Project type Is it an MSc, PhD, BSc(Hons) or PGDipSci? BSc(Hons) Advisers Who supervised/advised this student Coombs, D.S. Landis, C.A. Abstract The Abstract for this thesis A sequence of spilitic pillow lavas, pillow breccias and tuffs, cut by numerous dikes, which crops out over the eastern part of the peninsula is defined as the Riverton Volcanics. An overlying, poorly exposed, group of lithologies is mapped as Undifferentiated Permian. These two lithologic groupings are infaulted against fossiliferous tuffaceous metasediments belonging to the Greenhills Group. Two phases of dike intrusion are recognised. The earlier dikes are spilitic, in some cases feeders to pillow lavas. They are crosscut by porphyritic basaltic dikes, which also cut the Undifferentiated Permian lithologies. There are no dikes within the Greenhills Group rocks. Field and petrographic evidence suggests that the Riverton Volcanics were emplaced in shallow water. Partial analyses reveal a very low K20 content (average 0.15%) which cannot be readily explained in terms of metasomatism. These rocks are tholeiites and may represent oceanic crust. The andesitic to basaltic tuffs of the Greenhills Group show calc-alkaline affinities. Double grading within these rocks is explained in terms of shallow submarine eruption. The area has been burial metamorphosed to prehnite-pumpellyite and pumpellyite-actinolite facies. In the west, the Greenhills Group tuffs have been contact metamorphosed by the emplacement of the Longwood Intrusives. Fossil evidence indicates an upper Lower Permian (Mangapirian-Braxtonian) age for the Greenhills Group. The underlying rocks are placed in the lowest Permian but may be older. The association of calc-alka1ine tuffs and tholeiitic volcanics is explained in terms of a plate tectonic model in which the Undifferentiated Permian rocks, in part, represent continent-derived sediments. Department The department where the student is studying primarily. Geology Named locality Named locality describing the field area location. Riverton Peninsula Thesis description Number of pages, maps, CDs, etc. 92 leaves : illus., maps (fold.) Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Identifier An unambiguous reference to the resource within a given context 1973MacFarlane Creator An entity primarily responsible for making the resource Macfarlane, D. F., 1951- Date A point or period of time associated with an event in the lifecycle of the resource 1973 Title A name given to the resource Geology of the Riverton Peninsula, Western Southland Subject The topic of the resource Map Igneous petrology Metamorphic geology Structural geology Paleozoic Greenhills Group Permian Riverton Volcanics https://theses.otagogeology.org.nz/files/original/24438451e0d9206828554e765d2c1a03.pdf ea85ca099228c5b157350a1ca1df6ee4 Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Title A name given to the resource Geology theses OU Geology thesis Thesis or dissertation completed by University of Otago Geology students Location WKT (WGS84) The location stored in WKT (WGS84) format POLYGON ((168.074051681000014 -44.925488453999947,168.06958549400008 -44.931779880999954,168.067791513000088 -44.937080935999973,168.067194752000091 -44.938844997999979,168.067110221000121 -44.939093817999947,168.045070294000084 -45.004139145999943,168.038998114000037 -45.022035910999932,168.038281010000105 -45.024146320999932,167.998419775000116 -45.022717446999934,167.998122141000067 -45.022704570999963,167.972862057000043 -45.021789257999956,167.934813269000074 -45.020403230999932,167.941222882000034 -44.949907359999941,167.942878502000099 -44.931686147999983,167.944770442000049 -44.910838077999983,167.944922339000072 -44.910695966999981,168.009969203000082 -44.849492717999965,168.024092060000044 -44.836178357999984,168.02453317700008 -44.835760136999966,168.002592425000103 -44.822752441999967,167.988016037000079 -44.814104320999945,168.00462789900007 -44.799927073999982,168.013086319000081 -44.792702259999942,168.023030076000055 -44.795805424999969,168.032534198000121 -44.798767010999939,168.033542663000048 -44.79908095199994,168.078543978000084 -44.813105723999968,168.084082748000014 -44.793607572999974,168.08782644900009 -44.793767212999967,168.093405548000078 -44.797588447999942,168.117886105000025 -44.814341333999948,168.11579296900004 -44.835663550999982,168.11320202100012 -44.839939648999973,168.100595910000038 -44.861135933999947,168.093130446000032 -44.883703814999933,168.083760581000092 -44.911635544999967,168.083744295000088 -44.911828679999985,168.080796267000096 -44.91598086099998,168.074051681000014 -44.925488453999947)) Author last name Last name of the Author Williams Project type Is it an MSc, PhD, BSc(Hons) or PGDipSci? PhD Advisers Who supervised/advised this student Landis, C.A. Abstract The Abstract for this thesis In the upper Eglinton area, the Eglinton Volcanics (Permian) are intruded by plutonic rocks mapped as the Mackay Intrusives. A sharp fault contact separating the Eglinton Volcanics from crystalline rocks of the Fiordland Complex, i.e. separating New Zealand's eastern and western provinces is no longer recognised in this area and rocks mapped as Darran Doiorite by Wood (1962) are now mapped as Mackay Intrusives. The Eglinton Volcanics are mapped as two terranes separated by an elongate body of quartz-bearing diorite, the Mistake Diorite. The eastern (Plato) terrane, which consists largely or entirely of marine deposits, comprises a steeply dipping, east-younging sequence of volcanogenic sediments of basaltic to andesitic composition, intruded by abundant basaltic dikes. Four formations are defined: the basal (Gondor) formation consists of predominantly massive, coarse grained pyroclastic detritus and includes an Atomodesma limestone member; subsequent formations (Consolation, Divide and Fergus) are mainly of sand to silt grade rocks and include turbidites. Fossils from two new localities include brachiopods - Ambikella, Sulciplica transversa, Aperispirifer (?), Spir{ferellina and bivalves - Atomodesma marwicki, Etheripecten and Conocardium (?). They confirm an Early to Middle Permian age for the Plato terrane. Rocks of the western (Largs) terrane are largely of andesitic to dacitic composition and predominantly volcaniclastic, although massive andesite bodies are mapped at either end of the terrane. Fossils, limestones and turbidites are unknown, but strongly hematitic rocks, restricted to minor occurrences in the Gondor Formation of the Plato terrane, are common. The terrane may be partly of terrestrial origin. Basaltic andesite and andesite dikes are fairly common but several distinctive dike lithologies found in the Plato terrane, e.g. augite porphyrite, Cr-diopside ankaramite and microdiorite, are absent in Largs rocks. The southern part of the terrane appears to be folded into a tight syncline, however the structure is not completely resolved and formal formations have not been established. Age of the Largs terrane and its relation to rocks of the Plato terrane remains unknown. It is herein assumed to be of Early to Middle Permian age, though a younger, e.g. Mesozoic origin, cannot be discounted. Eglinton rocks are shown to be of tholeiitic to calc-alkalic affinity and are considered to be the products of Lower Permian island arc volcanism which accumulated either as separate arcs (i.e. Plato and Largs), or as separate portions of the same arc, approximately 180-190 km above a descending lithospheric plate. Low-grade burial metamorphism occurred, mainly during Permian time and parts of the Largs terrane have been hornfelsed during subsequent Mackay intrusion. Aspects of regional metamorphism are also recognised and this can probably be regarded as a Mesozoic development. Three metamorphic zones are mapped: a prehnite-pumpellyite-epidote zone (I) where metamorphic grade is prehnite-pumpellyite transitional to pumpellyite-actinolite schist facies; an actinolite-epidote zone (II) occurring west of zone I with assemblages of the chlorite zone of the greenschist facies; a biotite-actinolite-epidote zone (III) restricted to the northwestern part of the Largs terrane where the terrane is intruded by gabbroic and dioritic Mackay rocks. Mineral assemblages in zone III are compatible with those of the greenschist facies as well as the albite-epidote and hornblende-hornfels facies of contact metamorphism. Textural modification is not widely developed in either terrane. The Mackay Intrusives are subdivided into six units. The Gunn Dolerite comprises two intrusive bodies in the northern Plato terrane, its age is unknown but it may be as old as Early Permian. Mistake Diorite is the name given to the elongate, relatively homogeneous body of medium to coarse grained quartz-bearing diorite which separates the Largs and Plato terranes. K-Ar ages of 208, 208, 186, 182 and 180 m.y~ have been obtained from it and are interpreted as indicating a Triassic age of intrusion. The Hut Plutonic suite, comprising mainly white leuco-granite, flanks part of the western margin of the Mistake Diorite and is inferred to be of similar age to the Mistake body. Hollyford, Nurse and Glade suites are mapping units and are not necessarily of genetic significance, i.e. together they comprise a genetically related series of granitoid to gabbroic rocks characterised by diverse composition on outcrop scale, medium grainsize, zoned plagioclase and lack of widespread deuteric alteration. Each suite comprises a mappable rock mass in which one lithology or a narrow range of lithologies predominates. Leuco-gabbronorite predominates in the. Hollyford Gabbroic Suite, a unit mapped in the upper Hollyford area. Four K-Ar ages range from 130-136 m.y. (uppermost Jurassic to Cretaceous) and a cross-cutting trondhjemite dike gives concordant biotite and muscovite ages of 113 m.y. Rocks of the Nurse Plutonic Suite, mapped in the Nurse-Brandywine area, are granitoid to dioritic in composition. They are undated, but as rocks of identical composition and texture intrude Hollyford gabbronorites, a Cretaceous age seems likely. The Glade Plutonic Suite comprises texturally and compositionally diverse rocks in which dioritic types dominant. K-Ar ages of 189 and 112 m.y. on a hornfelsed andesitic inclusion recrystallised (?) leuco-granite respectively, suggest, in conjunction with field relations, a complex intrusive history. Microprobe analyses of rock forming minerals observed in a representative selection of plutonic and volcanic rocks are reported and discussed. In particular, Mg-Fe distribution coefficients (KD) have been calculated for coexisting pyroxenes from a series of gabbronorites across the Hollyford suite.KD changes systematically form east to west across the suite as the Fe:Mg ratio of the pyroxenes increases. This trend, and the concentration of olivine-bearing rocks in the eastern part of the suite, suggest that the gabbroic rocks may comprise a gravity-differentiated intrusion with its base towards the east. Several major north-to northeast-trending, high-angle faults are mapped. The Hollyford Fault marks the eastern margin of the Eglinton Volcanics and is considered to be a fundamental tectonic break. Skelmorlie Fault has offset Tertiary sediments of the Annick Group, perhaps by several kilometres in a sinistral strike-slip sense and/or by several hundred metres vertically (west side up). The Glade Fault, a newly described feature, has produced 5-6 km of apparent dextral offset in the Hut suite leuco-granite. The Eglinton Fault zone, mapped along part of the eastern margin of the Mistake Diorite, is characterised by gneissic mylonite containing sparse almandine garnet. A newly discovered sliver of Tertiary sediments faulted into the Plato terrane in Plato Creek, as well a.s Tertiary strata unconformably overlying Mackay and Eglinton rocks west of Mt Eglinton, are described briefly. Distinct differences in conglomerate provenance are noted within the Tertiary sequence near Mt Eglinton. Although a tectonic contact between New Zealand's eastern and western provinces is not recognised within the area mapped, it is concluded that the two provinces did not lie in their present relative position in the Permian and Early Mesozoic. If this conclusion is correct, then the present juxtaposition of the two provinces means that their mutual contact is, or was, tectonic. It is considered that the contact lies in approximately the same position as the median tectonic line as proposed by Landis and Coombs (1967) and that it has been subsequently obscured for most of its length by Mesozoic plutonism and Cenozoic tectonism and sedimentation. It is proposed that the term "median tectonic line" be retained for this contact between provinces of contrasted pre-Cenozoic geological evolution, notwithstanding the likelihood that the - contact probably originated as a zone of tectonised rock rather than as a sharp break, as originally mapped. OURArchive handle The handle from the Otago University Research Archive (OURArchive) <a href="http://hdl.handle.net/10523/5936">http://hdl.handle.net/10523/5936</a> OURArchvive access level Open Department The department where the student is studying primarily. Geology Named locality Named locality describing the field area location. Eglinton upper Thesis description Number of pages, maps, CDs, etc. 305 leaves : illus. (part col.) ; 29 cm. Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Identifier An unambiguous reference to the resource within a given context 1976Williams Creator An entity primarily responsible for making the resource Williams, John Greville. Date A point or period of time associated with an event in the lifecycle of the resource 1976 Title A name given to the resource Geology of the Upper Eglinton area : status of the median tectonic line. Subject The topic of the resource Map Geochemistry Igneous petrology Lithostratigraphy Mineralogy Paleozoic Eglinton Volcanics K-Ar dates Mackay Intrusives Median Tectonic Line Permian fossils https://theses.otagogeology.org.nz/files/original/36347101a27a15b68905c727936dc7ea.pdf 9f617ebdfb01bd850084f858164a0898 Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Title A name given to the resource Geology theses OU Geology thesis Thesis or dissertation completed by University of Otago Geology students Location WKT (WGS84) The location stored in WKT (WGS84) format POLYGON ((168.209693133000087 -45.665156176999972,168.188347208000096 -45.664532452999936,168.186946168000077 -45.6613425099999,168.180039790000023 -45.645621837999954,168.163645185000064 -45.608280301999969,168.163984342000049 -45.608294340999976,168.126187456000025 -45.504027253999936,168.129684672000053 -45.5041328099999,168.194297864000077 -45.506042373999946,168.198291142000016 -45.506157237999957,168.198741855000094 -45.506171281999968,168.316475437000122 -45.544962533999978,168.343043887000022 -45.553694694999933,168.338410751000083 -45.615379730999962,168.337693856000101 -45.615351159999932,168.337080913000023 -45.624312624999959,168.336980158000074 -45.624367193999944,168.321991751000041 -45.632687198999974,168.276571844000046 -45.657879342999934,168.260794339000086 -45.666619754999942,168.22099839100008 -45.665478830999973,168.210260803000097 -45.665170406999948,168.209693133000087 -45.665156176999972)) Author last name Last name of the Author Hyden Project type Is it an MSc, PhD, BSc(Hons) or PGDipSci? PhD Advisers Who supervised/advised this student Coombs, D.S. Abstract The Abstract for this thesis The West Dome sector of the Dun Mountain ophiolite belt has been mapped on a scale of 4 inches to 1 mile (approximately 1:16000). The area covers approximately 200 sq.km. (80 sq. ml.) and has been subdivided into northwest - southeast trending structural units that are correlated with the terranes of Coombs et al.(1976a). Minor but significant variations from this trend occur. Major faults are present at the contacts of these units. The following stratigraphy (from northeast to southwest) is recognised at West Dome: A. CAPLES - PELORUS TERRANE: This terrane contains sedimentary and igneous rocks which are in fault contact. Local informal nomenclature is proposed for these strata at West Dome. Acton Downs melange: This unit comprises tectonic inclusions of meta-igneous rocks and minor sedimentary ones that have undergone at least one period of cataclasis, set in an obscure matrix. Gyzeh volcanics: They contain mainly non-pillowed metabasalts and together with the Acton Downs melange, probably represent part of a much dismembered ophiolite sequence. Diston stream sedimentary unit: It can be subdivided into a lower, mainly coarse grained sandstone assemblage, and an upper, mainly fine grained assemblage of thinly interbedded fine sandstone and mudstone. B. HUMBOLDT GROUP: This group occurs as a dismembered ophiolite sequence at West Dome, the ultramafic portion giving rise to well developed knocker topography. Red Mountain Ultramafite: This subgroup is almost completely serpentinised and is present as a melange. The tectonic inclusions are dominated by metagabbros and metadolerites, but minor metabasalts rare sedimentary rocks and albite amphibolites occur in a serpentinite matrix. The meta-igneous rocks are derived from the overlying Livingstone Subgroup but the sedimentary inclusions, some containing Atomodesma, are of unknown origin. Livingstone Subgroup: This subgroup has been divided into four informal units of which units (ii) - (iv) are considered to be stratigraphically continuous and directly comparable with the upper part of an ophiolite sequence. unit (i) comprises non-pillowed metabasalts locally intruded by metagabbros. unit (ii) is dominated by metadolerites with minor amounts of metagabbros and metabasalts. Where contacts have been observed finer grained rocks intrude coarsed grianed ones. unit (iii) contains metadolerites and meta-pillow-basalt, the latter increasing in abundance stratigraphically upwards, and passing into unit (iv) in which meta-pillow-basalt and meta-pillowbreccia are present in subequal proportions. C. BRYNEIRA GROUP: This group has been redefined to include the following formations: Upukerora Formation: comprising basic volcanogenic conglomerates, sandstones and mudstones. Howden Formation: comprising limestones and basic volcanogenic sandstones and mudstones. Annear Formation: comprising significantly more quartz-rich sandstones and siltstones Tapara Formation: comprising basic volcanogenic sandstones, siltstones and claystones. This formation has been divided into eight informal units based on distinctive lithology. Winton Formation: comprising very thin interbedaed volcanogenic sandstones ru~d mudstones. D. STEPHENS GROUP: This is a new group uniting the Countess and Snowdon Formations. These formations have similar lithologies, mainly massive sandstones, with fewer thin mudstones and thick conglomerates, and indicate a notable change in depositional character from that of the underlying Bryneira Group. A Mid- to Late-Permian age for the sedimentary strata is suggested by the occurrence of Atomodesma trabeculum Waterhouse in the Diston stream sedimentary unit, by A. trechmanni Marwick in the Annear Formation, and a rich late Permian fauna at the top of the Countess Formation. This fauna includes fragments and moulds of brachiopods, corals, bivalves, gastropods, bryozoans, echinoderms and a trilobite. Calcite prisms, regarded as comminuted Atomodesma shells, are present in the Upukerora, Howden, Annear and Snowdon Formations, but more significantly, also in unit (iv) of the Livingstone Subgroup. Their presence strongly suggests a Permian age for the Humboldt Group. The major lithfacies recognised are conglomerate, sandstone, interbedded sandstone and mudstone, with minor amounts of limestone, pebbly sandstone and intraformational conglomerate. The lithofacies are considered to have been deposited in deep water by mass flow and turbidity currents. Modal analyses indicate the sandstones to be mainly lithic volcarenites derived from a basic to intermediate source area. The Annear Formation is exceptional because the sandstones are very significantly enriched in quartz. Bryneira and Stephens Group strata are considered to have been deposited in the axial trough of an elongate basin. Chemical analyses of red and non-red strata indicate that the red colouration varies with Fe2O3 FeO ratio. Red and non-red beds probably reflect variations in the palaeoclimate directly or indirectly attributable to Gondwanan Permian ice-age. Relict igneous minerals and ghost textures in the Red Mountain Ultramafite indicate a mainly harzburgite parent. Microprobe analyses of olivine, orthopyroxene and chromian clinopyroxene give compositions of Fo90 ; En90-92 ; Wo49 En48 Fs3 respectively and also indicate that the original opaque phase was chromian spinel. These values are directly comparable to mineral compositions from ophiolite sequences and Alpine - type ultrabasic complexes. Kizardite, chrysotile and magnetite are the major metamorphic minerals in the Red Mountain Ultramafite. Serpentinisation was probably initiated during an ocean-floor metamorphic episode, further alteration taking place during and possibly after the Rangitata Orogeny. The present mineral assemblage indicates temperatures of formation of less than 300°C and a few kilobars pressure, conditions that are comparable to those producing prehnite - pumpellyite facies assemblages in adjacent strata. Igneous textures are usually well preserved in the Livingstone Subgroup but metamorphic reconstitution is such that only three relict igneous phases now occur. Only Ca-rich pyroxene has been observed and it shows increasing alteration stratigraphically downwards, being most altered in the tectonic inclusions. Microprobe analyses of these clinopyroxenes indicate tholeiitic affinities for these rocks and using the criteria of Nisbet and Pearce (1977) the analyses suggest that the rocks were formed in an ocean-floor environment. Brown hornblende is restricted to the tectonic inclusions and is considered to have crystallised from an evolving magma. Opaque minerals invariably show alteration to sphene and this, together with microprobe data, indicates an original iron - titania oxide phase. Zeolite facies metamorphic assemblages in the southwest of the area pass northeastwards through a narrow zone of lawsonite - albite - quartz facies into an extensive area of prehnite - pumpellyite facies mineral assemblages. This low-grade regional metamorphism is associated with the Mesozoic Rangitata Orogeny. A temperature gradient of about 23C/km was operative during this event. Maximum pressures of approximately 5 kb and temperatures of approximately 380°C were attained. Prehnite - pumpellyite facies mineral assemblages overprint greenschist facies mineral assemblages in the metadolerites, metagabbros and albite amphibolites. Microprobe analyses of amphiboles from these rocks show a compositional gap within and between grains, but a miscibility gap is not developed. Amphibole compositions are governed initially by precursor mineral composition, later being modified by host rock composition. These results suggest that conditions of metamorphic equilibrium have not been attained. The meta-igneous rocks were metamorphosed under ocean-floor conditions of low pressure and of temperatures up to at least 400C, possibly reaching 600C locally. This metamorphic event was of an early Permian age, and was later overprinted during the Rangitata Orogeny. Co-existing phases in the Livingstone Subgroup include pumpellyite(Fe), albite, iron-rich epidote, chlorite, celadonite, prehnite, sphene, quartz and calcite. (Microprobe analyses are given for all but quartz and calcite). Andradite amd intermediate members of the andradite - grossularite series occur with prehnite, epidote, chlorite, quartz, calcite and an opaque phase in vesicle infillings of a non-pillowed metabasalt. Conditions of formation of this mineral assemblage involved temperatures of less than 300°C, possibly even less than 100C and pressue pressures of a few kilobars. Several models are discussed regarding the environment in which the strata at West Dome originated, and the ensuing tectonic conditions that brought about the juxtaposition of these rocks. The simplest model is that of a single Permian - Cretaceous volcanic arc - arc-trench gap - trench in which Humboldt Group (already metamorphosed under ocean-floor conditions) formed the upper plate of the subduction zone and on which Bryneira and Stephens Group strata were deposited in the arc-trench gap; Caples ·· Pelorus terrane rocks probably formed in part of the trench. All of these rocks were folded and regionally metamorphosed during the Mesozoic Rangitata Orogeny. Department The department where the student is studying primarily. Geology Named locality Named locality describing the field area location. West Dome Thesis description Number of pages, maps, CDs, etc. 178 leaves : ill., 3 maps (fold) ; 30 cm. Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Identifier An unambiguous reference to the resource within a given context 1979Hyden_G Creator An entity primarily responsible for making the resource Hyden, Graham. Date A point or period of time associated with an event in the lifecycle of the resource 1979 Title A name given to the resource Geology of the west dome sector of the Dun mountain ophiolite belt. Subject The topic of the resource Map Igneous petrology Metamorphic geology Sedimentology Paleozoic Atomodesma Dun Mountain Ophiolite ultramafic rocks https://theses.otagogeology.org.nz/files/original/c5b838b02251613ee177314dde89f0ef.pdf 9ec9ed52511a092de09f2ee6dcc3eb0e Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Title A name given to the resource Geology theses OU Geology thesis Thesis or dissertation completed by University of Otago Geology students Location WKT (WGS84) The location stored in WKT (WGS84) format POLYGON ((173.97229565724092 -41.446669091847582,174.069184461025344 -41.560201710849604,174.244061612668702 -41.744324060010733,173.981178710081792 -42.032833045685848,173.831129475729028 -42.291373711461993,173.620866779363666 -42.449973022459929,173.488073117236439 -42.750843279416173,172.905576474945121 -43.109238910458167,172.806984750851001 -43.437898220704461,173.00315742483653 -43.595298520423341,173.141366247133703 -43.823912405042165,172.825112002707442 -43.952506430896641,172.430788663956037 -43.808288792511618,172.093124085692409 -43.949041490626897,171.472661983822633 -44.228286102325747,171.285945581529063 -44.497185202336595,171.161700913624628 -44.638168019341407,171.168442109141523 -44.741888119651627,171.171424657224549 -44.806245822469563,171.1535253907048 -44.895275945329139,171.08477698981136 -44.997750881550701,169.753991870080739 -44.306691137287849,169.740593044953414 -44.099076280501457,169.967921891976999 -43.919541171841189,170.934762805348328 -43.308628836187793,171.310090376799451 -43.067016727290245,171.472393906654332 -42.943024367563723,171.722147129713477 -42.784067721669444,172.687041285245954 -41.949620115289662,172.875647451336704 -41.814144454524772,173.22874046976716 -41.673379737811153,173.540606229777552 -41.565093534123378,173.790403503033986 -41.49215209647781,173.784064700947766 -41.492195483636294,173.97229565724092 -41.446669091847582)) Author last name Last name of the Author MacKinnon Project type Is it an MSc, PhD, BSc(Hons) or PGDipSci? PhD Advisers Who supervised/advised this student Landis, C. A. Abstract The Abstract for this thesis Carboniferous to Lower Cretaceous Torlesse rocks and Haast Schist derivatives constitute the major part of the "eugeosynclinal" facies of the Eastern Province of New Zealand, Strata consist largely of quartzofeldspathic graywacke and mudstone, with minor but widely distributed conglomerate and associated volcanics, chert and limestone. Structure is complex; several periods of deformation are recognized; isoclinal and steeply plunging folds are widespread; and melange is present on both local and regional scales. Metamorphic grade is zeolite and prehnite-pumpellyite facies in the Torlesse and mainly pumpellyite-actinolite and greenschist facies in the schist. Fossils are sparsely but widely distributed. The bulk of the rocks fall into five areally extensive and mutually exclusive fossi1 zones: ·Atomodesma (Permian); Daonella (Middle Triassic); Torlessia (lower Upper Triassic?); Monotis (Upper Triassic); and combined Upper Jurassic-Lower Cretaceous zones. Contacts between major fossil zones are indeterminate and for the most part are probably tectonic. Structural and sedimentologic aspects of a small area (~6 sq km) of Monotis bearing Torlesse rocks near Arthurs Pass are described. Strata consist largely of sandstone-dominated sediment gravity flow deposits. Initial deformation probably began shortly after: deposition in Late Triassic times. Strata were folded and faulted and locally highly disrupted prior to a prehnite-pumrellyite metamorphic maximum in the Jurassic-Cretaceous. Sedimentologic columns from seven well exposed sequences on the South Island are described and interpreted in terms of depositional environments. Previous sedimentological studies are discussed, and a regional summary of Torlesse sedimentation on the South Island is presented. Strata are predominantly thick to very thick-bedded massive and graded sandstone with subordinate thinner bedded sandstone and mudstone deposited by turbidity currents and other types of sediment gravity flows in a deep marine environment. Overall sandstone:mudstone ratio is 2:1 to 3:1. In terms of submarine fan models, most strata are similar to middle and upper fan deposits. Mudstone-dominated slope, upper fan interchannel and lower fan-basin plain deposits are rare, except for Lower Cretaceous strata where lower fan-basin plain deposits are probably common. The Torlesse was not deposited as one large fan but consisted of a number of smaller sediment gravity flow deposits, not necessarily fan shaped, that were progressively accreted as deposition proceeded. Highly fossiliferous shallow- and non-marine deposits are present in a few areas of the Torlesse. Some are limestones deposited on local submarine highs. The others are clastic sequences of Middle Triassic and Jurassic age which rest unconformably on or in fault contact with Torlesse flysch. They are of limited areal extent and together occupy less than 1% of total Torlesse exposure on the South Island. Detrital mineralogy of Torlesse sandstones is largely preserved in zeolite and prehnite-pmnpellyite facies sandstones with low secondary matrix content. Potassium feldspar has been removed during metamorphism of some prehnite-pumpellyite and most higher grade sandstones. Petrographic analysis of 122 samples permit subdivision of Torlesse rocks into the following sandstone petrofacies: Q:F:L Lv/L %M P/F diagnositc heavy minerals Upper Jurassic-Lower Cretaceous 27:33:40 0.59 2.5 0.78 pumpellyite, prehnite Upper Triassic (Monotis) 35:42:23 0.73 3.5 0.78 - Lower Upper Triassic? (Torlessia) 31:59:10 0.73 4.7 0.78 - Middle Triassic (Daonella) 29:51:20 0.78 4.4 0.81 - Permian (Atm.) Caroboniferous? 24:50:26 0.92 1.6 0.81 - An additional petrofacies (Permian-fusiline, Q:F:L = 53:19:28, Lv/L= 0.81, %M = 0.4) is recognized for rocks within a small faultbounded sliver associated with Permian fusulines near Bemnore Dam. Granule and pebble-sized clasts from 17 Torlesse conglomerates are described petrographically. These comprise: sedimentary (58%) , most are cannibalistically reworked from older in-part metamorphosed Torlesse terrane, and a few are relatively mature quartz-rich sandstones including some quartz arenites; volcanics (20%), mainly rhyolite and dacite; quartzose and metamorphic (15%), mainly derived from metasedimentary terranes; chert (4%), some with radiolarians; and pluto11ic (3%) , mainly granodiorite to granite. Clast composition varies little with age, though Permian and some Middle Triassic conglomerates have fewer reworked Torlesse clasts and more quartz-rich sedimentary and basic-intermediate volcanic clasts than do younger conglomerates. The major source of Torlesse detritus was a continental volcano-plutonic arc and associated siliceous sedimentary and metasedimentary country rock coupled with an autocannibalistically reworked Torlesse source. Variations in detrital composition through time reflect changes in source terrane composition. From Permian-Carboniferous? through Late Triassic times a plutonic source was dominant, volcanism was variable, and reworking of Torlesse rocks, some of prehnite-pumpellyite facies, was minor but locally extensive. In Late Jurassic and Early Cretaceous times, the major sources were older. Torlesse rocks, including some textural grade 2 imd 3 Haast Schist, and acid volcanics. The inferred characteristics of the source terrane are compatible with a Western Province New Zealand - Gondwanaland source. In contrast to the quartzofeldspathic nature of the Torlesse, coeval sedimentary rocks of the Eastern Province are volcanogenic. They are thought to represent related forearc (Maitai-Murihiku terranes) and trench complex (Caples terrane) deposits derived from a volcanic island arc (Brook Street terrane). Petrographic analysis of 42 samples coupled with data from previous workers define the following petrofacies: Q:F:L Lv/L %M P/F Maitai-·Murihiku terranes, Permian-Lower Triassic 2:26:72 0.97 0.2 0.99 Murihiku terrane, Middle Triassic-Jurassic 11:40:49 0.90 1.0 0.85 Caples terrane Permian, Triassic? 7:26:67 0.94 0.3 0.93 In addition, low-lithic, high feldspar variants of the major Maitai-Murihiku petrofacies are recognized for some Permian (Annear Formation) and Jurassic sandstones. A reconstruction of New Zealand's Eastern and Western Provinces is presented. In Permian and Triassic times the Torlesse was deposited in trench-slope or borderland basins along a trench-transform margin fronting a continental volcano-plutonic arc source (Gondwanaland). Deposition was spasmodic but voluminous, and was accompanied by concurrent deformation and accretion resulting in parallel belts of Torlesse rock younqing outward from the Gondwanaland margin. Indurated and in-part metamorphosed Torlesse rocks were locally exposed to erosion in trench-slope-break or borderland settings with deposition of shallow marine and terrestrial deposits in these same areas during the Middle Triassic. At the same time, the Brook Street terrane volcanic arc and associated terranes were forming to the west of the Torlesse site, separated from Gondwanaland by a marginal sea. In latest Triassic or Early Jurassic times the Torlesse was rafted into the volcanic arc system via transform faulting roughly parallel to the Gondwana margin. The collision event resulted in tectonic thickening of Torlesse and Caples rocks at the plate interface and metamorphism to Haast Schist. The source was then dominated by older in-part metamorphosed Torlesse terrane, newly uplifted along the collision front, on which some Upper Jurassic shallow- and non-marine rocks were deposited. Closing of the marginal sea behind the Brook Street terrane in Late Jurassic-Early Cretaceous times resulted in juxtapositioning with the Western Province (Gondwanaland) along the Median Tectonic Line. Department The department where the student is studying primarily. Geology Named locality Named locality describing the field area location. South Island Arthurs Pass Thesis description Number of pages, maps, CDs, etc. 294 leaves : il. ; 30 cm. Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Identifier An unambiguous reference to the resource within a given context 1980MacKinnon Creator An entity primarily responsible for making the resource MacKinnon, Thomas Clark. Date A point or period of time associated with an event in the lifecycle of the resource 1980 Title A name given to the resource Sedimentologic, petrographic, and tectonic aspects of Torlesse and related rocks: South Island, New Zealand. Subject The topic of the resource Mesozoic Paleozoic Sedimentary petrology Sedimentology Tectonics sandstone petrofacies submarine fans Torlesse Supergroup https://theses.otagogeology.org.nz/files/original/1526f0d839e8b6317c72c87ad184a7fe.pdf dc920734dd7477260224ea6a82fc9ea3 Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Title A name given to the resource Geology theses OU Geology thesis Thesis or dissertation completed by University of Otago Geology students Location WKT (WGS84) The location stored in WKT (WGS84) format POLYGON ((168.194297864000077 -45.506042373999946,168.189013693000106 -45.516600855999968,168.178184152000085 -45.538238303999947,168.178056901000105 -45.538494454999977,168.155892306000055 -45.544517449999944,168.150250296000081 -45.546049912999933,168.129684672000053 -45.5041328099999,168.115751513000077 -45.475699618999954,168.120581391000087 -45.471200858999964,168.122549281000033 -45.469367653999939,168.185747213000013 -45.464576477999969,168.188225650000049 -45.474184185999945,168.195720533000099 -45.503198460999954,168.194297864000077 -45.506042373999946)) Author last name Last name of the Author Mackay Project type Is it an MSc, PhD, BSc(Hons) or PGDipSci? PGDipSci Advisers Who supervised/advised this student Norris, R.J. Abstract The Abstract for this thesis A small section of the Dun Mountain Ophiolite Belt is mapped in the Coal Hill area, Northern Southland. Ophiolitic rocks are present in two distinctively different melange belts, termed the Western Melange and the Eastern Melange. The Western Melange contains serpentinised ultramafite and microgabbro inclusions in a sheared serpentinite matrix. A large inclusion within this melange, termed the Coal Hill Inclusion, consists of spilite and associated volcanogenic sediments and is correlated with upper Livingstone terrane and basal Maitai Group, the Upukerora Formation. The Eastern Melange is characterized by a varied assemblage of rocks, including microgabbro, spilitic volcanic, conglomerate, sandstone, argillite and Atomodesmatinid limestone. A blue-grey Tertiary mudstone is also exposed in this Eastern Melange. A large sedimentary broken formation occurs within the Eastern Melange and is further broken to form part of the melange in the Windley River area. A small, coherent sliver of lower Livingstone microgabbro has a gradational contact with the Western Melange and is fault bounded to the west. This same fault also separates the melange units from Maitai Group rocks. The basal Upukerora Formation consists mainly of polymict breccias, together with minor interbedded sandstones and limestones. Stratigraphically overlying the Upukerora Formation is the Tramway Formation, composed of fine, grey sandstones and uncommon tuffs and associated arkosic rocks. Two infaulted slivers of Tertiary rocks are mapped in the area. Lithologies include fine, grey sandstones, occasionally with pebbly layers and a probable non-marine rock, with lignitic layers and lenses. Department The department where the student is studying primarily. Geology Named locality Named locality describing the field area location. Coal Hill Thesis description Number of pages, maps, CDs, etc. 200 p. : ill., maps ; 30 cm. Dublin Core The Dublin Core metadata element set is common to all Omeka records, including items, files, and collections. For more information see, http://dublincore.org/documents/dces/. Identifier An unambiguous reference to the resource within a given context 1982Mackay Creator An entity primarily responsible for making the resource Mackay, Duncan Ross. Date A point or period of time associated with an event in the lifecycle of the resource 1982 Title A name given to the resource Geology of Coal hill. Subject The topic of the resource Map Paleozoic Igneous petrology Metamorphic geology Structural geology Maitai Group melange ophiolite