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732


Journal of Paleontology 89(5):730–747


heterozooecia and acanthostyles surrounding each autozooecial aperture, and wall thickness in the exozone were determined. The spacing of structures is measured as the distance


between their centers. Statistics were summarized using arith- metic mean, sample standard deviation, coefficient of variation, and minimum and maximum values. The Geosciences Society of New Zealand operates a


national database of fossil localities, the New Zealand Fossil Record File, and a similar file has been established, based in the School of Environment, University of Auckland, for New Caledonian fossil collections held in New Zealand institutions. The New Caledonian Fossil Record File uses a running number prefixed by ‘NC’ and ‘f,’ as in ‘NC/f302,’ and this system, often with the ‘NC’ omitted, will be used in this report. Additional catalog systems are used to denote collections


Figure 2. Correlation of the New Zealand local chronostratigraphic scheme with the international scheme (after Cooper, 2004; and GNS Science, 2012), with the taxa on which each local stage/substage is based. Included are the map symbol for each local stage (e.g. Br = Oretian) and dates for stage and zone boundaries; Ma = millions of years (after Cooper, 2004). As noted in the text, the local scheme is applied also in New Caledonia.


with the base of the Rhaetian. It was earlier suggested (Zhang and Grant-Mackie, 2001) from palynological evidence that the Triassic-Jurassic boundary lay within the upper part of the Otapirian stage, but it is now recognized that the turnover in terrestrial flora from Triassic to Jurassic occurred a little earlier than that in the marine realm (Palfy et al., 2000; Hesselbo et al., 2002), and the top of the Otapirian is now regarded as equating with the top of the Triassic in New Zealand (Cooper, 2004; GNS Science, 2012).


Materials and methods


Since the mid-1960s, members of the Department of Geology (now included in the School of Environment), University of Auckland, New Zealand, have worked in New Caledonia in collaboration with the Bureau de Recherches Géologiques et Minières, Orléans, France, among other projects, mapping the Téremba Terrane and studying its biota. Extensive paleontolo- gical collections were built up in Auckland as a result and these form the basis for the present study. Bryozoan specimens have been selected from these collections and sent initially to PS in Kiel, where many have been cut and glass-mounted slides or acetate peels made for microscope analysis and photography. Bryozoans were investigated in thin sections using


binocular transmitted light microscopy. Morphologic character terminology is partly adopted from Anstey and Perry (1970). The following morphologic characters were measured and used for statistics in the studied material (Fig. 3). Branch diameter, exo- (endo-) zone width, autozooecial


aperture width and spacing, acanthostyle diameter, hetero- zooecia diameter, autozooecial diaphragm spacing, number of


and for individual specimens, especially type and figured material. These are usually alphanumerics, as follows: ‘AU’ and a running number denotes a collection held in the School of Environment, University of Auckland; ‘J’ and a running number is for individual specimens in the catalogue of type and figured bryozoans of that same institution; ‘GS’ and a running number denotes a collection held by GNS Science, Wellington. Where specimens are now represented by multiple fragments (slides, peels, off-cuts), the specimen number is extended with a lower- case letter (a, b, c,…) as a suffix. Bryozoans come from three parts of the outcrop area of the


Téremba Terrane: from the Moindou-Téremba area in the northwest (Campbell and Grant-Mackie, 1984; Campbell et al., 1985), from Ile Leprédour in northwestern Baie de St-Vincent (Pharo, 1967), and from Iles Ducos, Hugon, and Page, and Ilot Turpin in central Baie de St-Vincent. This is not to say that they may not be found in other parts of this terrane; it only indicates their absence from collections. The oldest bryozoan-bearing strata occur in the Moindou-


Téremba area. The Ouarai Formation consists of 140–180m of dark volcaniclastic rudites, arenites, and minor tuffs lying unconformably on Early Triassic Moindou Formation and overlain unconformably by Ouamoui Formation (Campbell et al., 1985). Rare bryozoans are found in argillites within a 30-m-thick sequence dominated by coarse sandstones and fine rudites in the lower quarter of the formation on the Téremba coast about 2 km south of an old wharf (Fig. 4). They occur as small cylindrical branch fragments up to 6mm long. The Ouamoui Formation is approximately 90m thick in the


vicinity of Mé Ouamoui, where it contains Bryozoa (it reaches 395m thick within the Moindou-Téremba area) and consists of


well-bedded fossiliferous coarse to fine volcaniclastic arenites fining upward to more common lutites, and includes minor rudites in the lower part and tuffs throughout (Campbell et al., 1985). This sequence is unconformably overlain by the Leprédour Shellbeds. Rare bryozoans have been collected from one level in medium to coarse sandstones 15–20m from the top and consist of small fragments of delicate branching type. The small collection was unfortunately misplaced in transit and is not included in this report. The Leprédour Shellbeds are a sequence of well-bedded


fine to coarse volcarenite shellbeds with minor rudites and lutite units, coquina limestones, and tuffs all dominated by the highly gregarious bivalve Monotis. On Ile Leprédour they reach a thickness of 470 m, with an unknown relationship with


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