Use policyThe full-text may be used and/or reproduced, and given to third parties in any format or medium, without prior permission or charge, for personal research or study, educational, or not-for-prot purposes provided that:• a full bibliographic reference is made to the original source • a link is made to the metadata record in DRO • the full-text is not changed in any way The full-text must not be sold in any format or medium without the formal permission of the copyright holders.Please consult the full DRO policy for further details. Zealand archipelago: the northern North Island (including Northland, Auckland, and the Coromandel 13 Peninsula); the southwest coast of the North Island; the Canterbury coast (South Island); and the 14 Otago coast (South Island). In the North Island the RSL highstand commenced c. 8,100-7,2400 cal yr 15 BP when present mean sea-level (PMSL) was first attained. This is c. 600-1,400 years earlier than has 16 been previously indicated for the New Zealand region as a whole, and is consistent with recent 17Holocene RSL reconstructions from Australia. In North Island locations the early-Holocene sea-level 18 highstand was quite pronounced, with RSL up to 2.75 m higher than present. In the South Island the 19 onset of highstand conditions was later, with the first attainment of PMSL being between 7,000-20 6,400 cal yr BP. In the mid-Holocene the northern North Island experienced the largest sea-level 21 highstand, with RSL up to 3.00 m higher than present. This is demonstrably higher than the 22 highstand recorded for the southwest North Island and Otago regions. A number of different drivers 23 region, while research from Australia has suggested that north-south variations in Holocene RSL 32 changes due to hydro-isostatic influences are limited or non-existent. At the regional-to local-scale, 33 post-glacial meltwater loading on the continental shelf around New Zealand is predicted by GIA 34 modelling to have a significant effect on the timing and magnitude of RSL changes through the 35 phenomenon of continental levering. The spatial variation in continental levering is controlled by the 36 configuration of the coast and the width of the adjacent continental shelf, with continental levering 37 providing a robust explanation for the observed spatial and temporal variations in RSL changes. 38Further research is required to characterise the regional and local effects of different tectonic 39 regimes, wave climates, and sediment regimes. These are potentially very significant drivers of RSL 40 variability at the regional-to local-scale. However, the magnitude of their potential effects remains 41 equivocal. 42Highlights 43  RSL histories were reconstructed for four regions in the New Zealand archipelago 44  Northern sites experience RSL rise earlier compared to southern sites 45  Northern sites experience a higher-magnitude highstand compared to southern sites 46  Long-wavelength signals from Antarctica cannot explain the observed variation in RSL 47  A range of processes potentiall...

No abstract

No abstract

No abstract

This paper presents a systematic review and correlation of river terraces identified in 44 river catchments in the North Island, New Zealand, to assess river behaviour over the last c. 30 000 yr. This provides a comprehensive foundation from which to assess controls on river dynamics over this critical period of landscape development from the last glacial through to the present interglacial. From this review, an integrated framework for elucidating fluvial responses to environmental change is proposed. Sensitivity of river systems to climate change is variable over this timescale. Substantial sediment inputs to valley floors during the last glacial reduced sensitivity to subtle climatic shifts. Sensitivity increased during the Holocene, with terraces forming in response to episodes of storminess. Tectonics and volcanic activity may both override climatic forcing to cause either cutting or filling of the valley floor.