[en] One of the key dating methods used in paleoclimate research utilizes the natural radioactive decay of uranium to thorium in archives containing U-bearing minerals, such as the calcium carbonate forming the skeletons of fossil corals and speleothems. More specifically, this chronometer, commonly referred to as the U-series dating method, is based on the decay of ²³⁸U to its longest-lived intermediate daughters, ²³⁴U and ²³⁰Th, and subsequent decay through to stable isotopes of Pb. It is the respective 250,000 and 75,000 year half-lives of these daughter isotopes, which make the U-series system particularly useful for dating Quaternary climate events spanning the last 600,000 years of Earth's history. The U-series thus bridges the gap between the ∼45,000 year upper limit of conventional radiocarbon dating and the ∼200,000 year lower limit of K-Ar and ⁴⁰Ar-³⁹Ar dating. 2 refs., 5 figs

[en] The Conventional Radiocarbon Age does not give an accurate estimate of the age, and must be corrected for the mean life and the actual ¹⁴C levels in the past environment. This correction is the process we call 'calibration'. 1 ref., 11 figs

[en] In 1936, Alfred Nier produced the first precise measurement of isotope abundance ratios and his design still remains the basis of stable isotope mass spectrometry. Stable isotope measurements have been applied to many fundamental problems in geochemistry, petrology, and paleoclimatology. These applications can be broadly classified into four main types: thermometry, tracers, reaction mechanisms, and chemostratigraphy. 56 refs., 11 figs., 2 tabs

[en] Is is possible to measure nearly any type of sample for almost any element with little or no preparation, especially if the sample is vacuum compatible. Besides solid state samples, examples include powders, rocks, particulate matter on filters, chemical precipitates on filters, artefacts and biological samples such as bone, teeth and shells. Samples as small as 10 micro-m can be measured with the proton microprobe IBA facility which is unique in New Zealand. 7 refs., 11 figs., 4 tabs

[en] Useful tools for determining absolute ages of sediments deposited within the last c. 100 years include ²¹⁰Pb, ¹³⁷Cs, and bomb radiocarbon. Cosmogenic ³²Si, with a half life of c. 140 years, can be applied in the age range 30-1000 years and is ideally suited for this time period. Detection of ³²Si is, however, very difficult due to its extremely low natural specific activity, and the vast excess of stable silicon (i.e. low ³²Si/Si ratio). 23 refs

[en] Ice cores from New Zealand and the Antarctic margin provide an excellent means of addressing the lack of longer-term climate observations in the Southern Hemisphere with near instrumental quality. Their study helps us to improve our understanding of regional patterns of climate behaviour in Antarctica and its influence on New Zealand, leading to more realistic regional climate models. Such models are needed to sensibly interpret current Antarctic and New Zealand climate variability and for the development of appropriate mitigation strategies for New Zealand. (author). 27 refs., 18 figs., 2 tabs

[en] This is a brief introduction to radiocarbon dating, complete with a short glossary of radiocarbon terms. 13 refs., 4 figs

[en] The paper covers: a bit of basic physics; underlying principles of cosmogenic isotope techniques; atmospheric ¹⁰Be and ⁷Be; in situ ¹⁰Be, ²⁶Al, and ¹⁴C. 9 refs., 2 figs

[en] Compilation of abstracts drawn from published and unpublished papers which describe the following topics: ¹⁰Be/⁹Be variations in Pleistocene cyclothems; ¹⁰Be/⁹Be variations in loess; ¹⁰Be/⁹Be dating of Fe-Mn nodules and crusts; ¹⁰Be/⁹Be dating of Antarctic soils; ¹⁰Be and ⁷Be flux rates in rain; ¹⁰Be/⁹Be dating of deep-sea sediments; SED of up-lifted marine terraces. Refs., 8 figs

[en] Ion beam analysis (IBA) techniques at GNS are used to (1) analyse for elemental compositions of rock powders and minerals including coal, (2) determine fine-scale elemental distributions in glass, individual minerals and whole rocks using imaging, line-scanning or point analyses and (3) probe compositions of buried structures in polished rock sections such as fluid and melt inclusions including daughter minerals in fluid inclusions. Apart from these, IBA techniques are also used (1) for standard-independent hydrogen detection and profiling at ppm levels (e.g. elastic recoil detection analysis or ERDA) and elemental depth profiling (Rutherford backscattering or RBS), (2) to probe lattice residence of major and minor trace elements and (3) to map zonation of certain ions, such as REE, in minerals using ionoluminescence (IL) or a combination of cathodoluminescence and PIXE. (author). 84 refs., 9 figs