50thKaikoura05 -1- Kaikoura 2005 CHARACTERISATION OF NEW ...

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It is probable that the specimen was collected by Fleming during a field excursion organised during the 11 th Annual Geological Survey Staff Conference, held at Kaikoura between the 10 th and 16 th May 1955. The excursion, on Thursday the 12 th May, planned to visit Haumuri Bluff between 2 and 4pm and then pass by Mikonui Stream on the way back to the meet the bus at Oaro. This particular conference is also of note historically; as it was during this conference the inaugural meeting of the New Zealand Geological Society was held (Hayward 1980) This specimen is the first pterosaur bone recorded from the South Island of New Zealand. It also represents the earliest verifiable collection of a Mesozoic terrestrial vertebrate in New Zealand, predating Dr. Joan Wiffen’s dinosaur discoveries by more than 20 years. Unfortunately it was not recognised for what it was for almost 50 years. J. Crampton, T. Mumme, I. Raine, L. Roncaglia, P. Schiøler, G. Turner and G. Wilson, 2000. Revision of the Piripauan and Haumurian local stages and correlation of the Santonian-Maastrichtian (Late Cretaceous) in New Zealand. New Zealand Journal of Geology and Geophysics 43:309-333 G. Warren and I. Speden, 1978. The Piripauan and Haumurian Stratotypes (Mata Series, Upper Cretaceous) and correlative sequences in the Haumuri Bluff District, South Malborough (S56). New Zealand Geological Survey Bullentin 92. 60p B. Hayward. 1980 The first 25 years – A brief history of the Geological Society. Geological Society Newsletter No 50: pg6-14. POSTER THE RELATIONSHIP BETWEEN THE CAPLES AND DUN MOUNTAIN TERRANES Dushan Jugum & Richard J. Norris Geology Department, PO Box 56, University of Otago, Dunedin (dushan*geology.co.nz) Geochemical and structural data will be presented to help interpret the melanged boundary between the Caples and Dun Mountain Terranes. Preliminary data indicates that: 1. The Windon Melange extends from the East Eglinton to Windley Rivers in Southland (approx. 54 Km) and its geochemistry and lithology are distinct from the Dun Mountain Ophiolite. The Windon Melange is fault 2. bounded and is located to the east of the Dun Mountain Ophiolite. There is no reason to separate the Harris Saddle and the West Burn Formation of the Caples Terrane as they share stratigraphical location, lithology and igneous geochemistry. 3. This composite formation occurs to the east of the Windon Melange, however small fault blocks have been found between the Windon Melange and the Dun Mountain Ophiolite. The Patuki Melange of Nelson and the Windon Melange of Southland can be considered to be of identical origin. 4. There is no visible evidence for an original relationship between the Greenstone 5. (Croisilles) Melange and the Windon (Patuki) Melange. The Dun Mountain Ophiolite, although block faulted and internally sheared is not melanged, away from major bounding fault zones. Where these terranes are out of their normal order, a model of flexural strike slip due to the Cenozoic dextral movement in the South Island is proposed for their emplacement. This modal has already been proposed to explain repeated lithologies near West Dome (Cawood, 1986) and here the idea will be expanded to include the Livingstone Mountains and the Red Hills in Nelson, with cooperating structural evidence. It has also been observed that the active part of the boundaries between these units has shifted several times. The different strengths of serpentinite and ultramafic rock are manifested in the distribution of strain along the Dun Mountain Ophiolite. This has a significant effect on the current pattern of New Zealand’s geology. One of the more significant examples is a bend in the Dun Mountain Ophiolite and neighbouring terranes of approximately 45 o near the Red Hills in Nelson. POSTER GONE BUT NOT FORGOTTEN - CASUALTIES OF THE LAST GLOBAL EXTINCTION Shungo Kawagata 1 , Bruce W. Hayward 1 , Hugh R. Grenfell 1 & Ashwaq T. Sabaa 1 1 Geomarine Research, 49 Swainston Rd, St Johns, Auckland (s.kawagata*geomarine.org.nz) The extinction of a group of elongate, cylindrical deep-sea benthic foraminifera occurred during the mid-Pleistocene Climatic Transition (MPT), between 1.2 and 0.55 Ma. This extinction was first recognised ~25 years ago and until recently its full impact was undocumented. Our studies in eighteen ODP cores from the North Atlantic, South Atlantic, Caribbean, Mediterranean, Southern Ocean, North Indian, South China Sea and South-west Pacific, show that at least 82 species and 17 genera became extinct during this period of major global climate and oceanographic change. A further 4 species and 3 genera declined dramatically during the MPT, but 50 th Kaikoura05 -40- Kaikoura 2005
survived through in low numbers in geographicallyrestricted refugia. One complete family (Stilostomellidae – 21 species), characterised by an unusual tooth structure in its necked aperture, became extinct at this time; and a second family (Pleurostomellidae – 24 species), also characterised by unusual elliptical or hooded apertures, was killed off except for two species that appear to have just survived through. A further 30 species in the large Nodosariidae family also died out and most of these too, had unusual cribrate or narrow, constricted apertures. Prior to the MPT, many of the extinct species had cosmopolitan distributions at middle bathyal to upper abyssal depths (600-3000 m), although a minority had geographically-limited distributions. Our studies indicate that ~20% of the global diversity of benthic foraminifera at these depths (excluding the diverse unilocular taxa) became extinct during the MPT. This was an extinction rate of ~30% of the middle bathyal-upper abyssal fauna/myrs, which is an order of magnitude greater than the background extinction rate for deep-sea benthic foraminifera of ~2-3%/ myrs. ORAL “CM/YR” IS NOW AVAILABLE – WHAT OF THE NEXT 50 YEARS? David Kear 34 West End, Whakatane (kear*xtra.co.nz) In its first 50 years, our Society exceeded all expectations and world geology underwent its greatest revolution. Belief in the Alpine Fault led to that in Continental Drift, which sparked off a new era of Plate Tectonics with a new unit for its movements of “cm/yr”. There seems general acceptance of these concepts in NZ, regarding other parts of the world. Let us hope that the next 50 years will bring comparable acceptance regarding NZ itself. Conclusions involving “plate tectoniclike” movements by many authors have been commonly ignored in appropriate diagrams and papers – by various means ranging from denying all discussion, to preferring a belief in zero-movement. Plate tectonic conclusions, many dating back over decades rather than years, that seem not to be fully accepted in general papers (or need more convincing reporting?), include: �Northland Allochthon it took half those 50 years, for even discussion to be acceptable. �Central Volcanic Region (CVR) was created from nothing since 2.5 Ma, along with the Havre Trough. Stern’s diagram illustrating that situation is nearly 20 years old. �Alpine Fault was active in both North and South Islands up to ca 5 Ma (major North Island faulting has long been widely noted and joined commonly to the Alpine Fault); its trace is now precisely located as the CVR’s boundary, & could become widely adopted. � Offshore Northland has been shown to have moved southeast between 15 & 5 Ma to become the East Coast - in many publications dating back between 10 and 38 years. �Whakatane was moved southeast at 2�cm/year for 400 k.yr (evidence 10+ years old). �Clockwise North Island Rotation since 15 Ma – a 30 year-old average of 65 o has been supported recently, but the effects of rotation are seldom considered in general papers. � Three North Island “Tectonic Events” (ca 10 m.yr apart since 25 Ma) have been named, but ignored, for ca 10 years; they allow changes in compression & tension to be dated accurately and linked to (e.g.) important changes in the local class of volcanism. � A Single Subduction System, initially off Northland, moved & rotated progressively via Coromandel offshore, to become the Hikurangi Subduction System with only one change in the rotation rate at a tectonic event. No new data are necessarily needed to reach such conclusions as these. A 1963 diagram, based solely on then published (pre- radiometric) data, nevertheless illustrated the creation of the CVR from nothing. The North Island predominates in these examples, but the 2005 fieldtrip programme emphasises an accelerating interest in Marlborough’s plate tectonic history - reflected in several recent convincing papers. Compatibility of evidence from the two islands, at specific points backwards in time, will be a key objective for the second 50 years – Alpine Fault movement, large rotation, tectonic events, subsurface termination of subduction, effects on non-geologic factors etc. However the overwhelming need will be to promote a greater acceptance of the reality of NZ Plate Tectonics, in both thinking and writing. Should that be achieved, the next 50 years will be as exciting and rewarding scientifically for the next generation as the last 50 years have been for us, and NZ will once again stimulate world thinking about the revolutionary science of plate tectonics. ORAL 50 th Kaikoura05 -41- Kaikoura 2005
Page 1 and 2: CHARACTERISATION OF NEW ZEALAND NEP
Page 3 and 4: myrtaceous. One 20 mm diameter flow
Page 5 and 6: ange of lower resolution or fragmen
Page 7 and 8: CRETACEOUS-EOCENE TRANSGRESSION MAR
Page 9 and 10: consists of a well-developed canyon
Page 11 and 12: model. The relative position of the
Page 13 and 14: converts to plate theory. Thus, the
Page 15 and 16: and on the following morning the mi
Page 17 and 18: the LGM grass peak. This period of
Page 19 and 20: offshore west coast to offshore eas
Page 21 and 22: 4 Institut de Recherche pour le Dé
Page 23 and 24: VEGETATION AND CLIMATE CHANGE AT TH
Page 25 and 26: wider range. The youngest layer has
Page 27 and 28: few normal faults visible especiall
Page 29 and 30: TRACKING CRUSTAL DIFFERENTIATION AN
Page 31 and 32: EMPIRICAL SCALING RELATIONS FOR SEI
Page 33 and 34: hydrovolcanic eruptions then took p
Page 35 and 36: and that the MTL marks a Late Carbo
Page 37 and 38: faunal changes within these cores w
Page 39: material at subsurface depths of se
Page 43 and 44: in the TVZ and southern Havre Troug
Page 45 and 46: Tephra beds are commonly used to ai
Page 47 and 48: The MCC is bounded by deep-seated t
Page 49 and 50: distal alluvial plains where large
Page 51 and 52: Many of the molluscs in the highly
Page 53 and 54: incremental slip history and paleoe
Page 55 and 56: This paper explores what we know of
Page 57 and 58: volcanism and a linear vent oriente
Page 59 and 60: These areas are also described in
Page 61 and 62: 3D IMAGING OF THE FORE- AND BACKTHR
Page 63 and 64: ascending methane fluids/gases of p
Page 65 and 66: THE GRIFFENS ROAD TEPHRAS: VALUABLE
Page 67 and 68: sideritic concretions that occur in
Page 69 and 70: with 63.8%, and then [3] with 49.9%
Page 71 and 72: U-Th-Ra disequilibria data. In part
Page 73 and 74: landslide tsunami in the past. Rece
Page 75 and 76: core complex mode, temperature driv
Page 77 and 78: truncating three plutonic suites of
Page 79 and 80: active, andesitic White Island volc
Page 81 and 82: and voluminous than at any on Earth
Page 83 and 84: oundaries and with immature source
Page 85 and 86: The new era of commercial viability
Page 87 and 88: TECTONICS OF THE GALATEA BASIN USIN
Page 89 and 90: performed by the electron backscatt
Page 91 and 92:
25km northeast of the volcano. Alth
Page 93 and 94:
Most of the tectonic blocks in the
Page 95 and 96:
TECTONIC AND NON-TECTONIC CAUSES OF
Page 97 and 98:
The continental shelf of the Povert
Page 99 and 100:
5 Dept. of Mineral Sciences, Smiths
Page 101 and 102:
Adams CJ...........................
Page 103 and 104:
Naish T............................
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