Downwasting of the Tasman Glacier, South Island, New Zealand: Changes in the terminus region between 1971 and 1993

Hochstein, M. P.; Claridge, David; Henrys, Stuart; Pyne, Alex; Nobes, David C.; Leary, S.F.

doi:10.1080/00288306.1995.9514635

Cited by 54 publications

(35 citation statements)

References 29 publications

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“…9) for a single year DEM difference and ±3.5 m yr −1 for a 6 year difference. For the glaciers on the east side of the divide, elevation change rates of the tongue have been ≈ −1 m yr −1 between 1890-1964/1971(Skinner, 1964Hochstein et al, 1995) and more recently up to −4.5 m yr −1 from 1986-1990(Quincey and Glasser, 2009. This is at the limit of what can be detected given the data in Table 1.…”

Section: Glacier Elevation Changesmentioning

confidence: 99%

Co-registration and bias corrections of satellite elevation data sets for quantifying glacier thickness change

2011

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Abstract.There are an increasing number of digital elevation models (DEMs) available worldwide for deriving elevation differences over time, including vertical changes on glaciers. Most of these DEMs are heavily post-processed or merged, so that physical error modelling becomes difficult and statistical error modelling is required instead. We propose a three-step methodological framework for assessing and correcting DEMs to quantify glacier elevation changes: (i) remove DEM shifts, (ii) check for elevation-dependent biases, and (iii) check for higher-order, sensor-specific biases. A simple, analytic and robust method to co-register elevation data is presented in regions where stable terrain is either plentiful (case study New Zealand) or limited (case study Svalbard). The method is demonstrated using the three global elevation data sets available to date, SRTM, ICESat and the ASTER GDEM, and with automatically generated DEMs from satellite stereo instruments of ASTER and SPOT5-HRS. After 3-D co-registration, significant biases related to elevation were found in some of the stereoscopic DEMs. Biases related to the satellite acquisition geometry (along/cross track) were detected at two frequencies in the automatically generated ASTER DEMs. The higher frequency bias seems to be related to satellite jitter, most apparent in the backlooking pass of the satellite. The origins of the more significant lower frequency bias is uncertain. ICESat-derived elevations are found to be the most consistent globally available elevation data set available so far. Before performing regional-scale glacier elevation change studies or mosaicking DEMs from multiple individual tiles (e.g. ASTER GDEM), we recommend to co-register all elevation data to ICESat as a global vertical reference system.

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Section: Glacier Elevation Changesmentioning

confidence: 99%

Co-registration and bias corrections of satellite elevation data sets for quantifying glacier thickness change

2011

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“…The dataset obtained for these three lakes is similar to that obtained for Tasman Lake by Hochstein et al (1995), so this discussion addresses all four lakes. All the lakes so far studied exhibit marked similarities, in both qualitative and quantitative characteristics, but also some interesting contrasts.…”

Section: Discussionmentioning

confidence: 66%

“…Tasman Lake is almost isothermal like Maud and Godley lakes, with a temperature range of just 0.2°C, and, like Hooker Lake, it is very cold with absolute temperatures everywhere <0.5°C (Hochstein et al 1995). However, such low temperatures contrast with those in Maud and Godley lakes, and, unlike Hooker Lake, there is no thermocline.…”

Section: Lake Temperaturesmentioning

confidence: 97%

“…1 ). The limnology of Tasman Lake has recently been studied by Hochstein et al (1995), and reconnaissance observations were carried out at Tasman Lake by the present authors in 1994,1995, and 1997. The glaciers which terminate in these lakes are all mantled by up to 2 m of coarse supraglacial debris (Kirkbride 1993(Kirkbride , 1995, including deposits of large rock avalanches (Kirkbride & Sugden 1992;McSaveney 1992a, b;Evans & Clague 1994).…”

Section: Field Areamentioning

confidence: 99%

“…Cirque lakes are dammed by rock bars or terminal moraines, and valley-floor lakes are dammed by moraines and/or outwash heads (Gage 1975). Only two ice-contact lakes have been studied previously in detail (Table 1): Ivory Lake (Anderton & Chinn 1978;Hicks et al 1990), and the much larger Tasman Lake (Hochstein et al 1995). Apart from these studies, and the documentation of the rate of growth of ice-contact lakes in Mt Cook National Park by Kirkbride (1993), the characteristics of these dynamic systems remain unknown, although some of New Zealand's large, distal, glacier-fed lakes and their environs have received detailed attention (Irwin 1972;Gage 1975;Jolly & Irwin 1975;Irwin & Pickrill 1982;Pickrill & Irwin 1983;McGowan et al 1996).…”

Section: Introductionmentioning

confidence: 99%

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Temperature and bathymetry of ice‐contact lakes in Mount Cook National Park, New Zealand

Warren¹,

Kirkbride²

1998

New Zealand Journal of Geology and Geophysics

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Several ice-contact lakes have formed in conjunction with twentieth century glacier retreat in Mt Cook National Park. They occupy overdeepened glacial valleys and are dammed by terminal moraines and/or outwash heads. During the autumns of 1994 and 1995, the temperature and bathymetry of "Maud lake", "Godley lake", and Hooker Lake were surveyed. The near-glacier vertical water temperature profiles exhibited greater temperature variation than those at the distal ends of the lakes. Thermal stratification existed in Hooker Lake, whereas both Maud and Godley lakes were thoroughly mixed. Water temperatures in the latter were consistently between 3 and 4.5°C, but most parts of Hooker Lake were cooler than 2°C, with a minimum recorded temperature of 0.2°C. These contrasts are important because melting of submerged parts of glacier termini is significant for ablation rates and for the dynamics of calving termini. All the lakes are steep sided and deep. Maud and Godley lakes approach 100 m in depth, whereas Hooker Lake has a maximum recorded depth of 136 m. Extensive flat floors in Maud and Godley lakes probably reflect rapid sediment accumulation following glacier retreat. Water depth at the termini of iceberg-calving glaciers is known to correlate strongly with rates of iceberg production and hence the rate of glacier retreat. However, given the substantial water depths through which these glaciers (and also the neighbouring Tasman Glacier) have retreated, they appear to be more stable than comparable glaciers in other countries. The subaqueous geometry of all the glacier termini comprises a projecting ramp of glacier ice. All the lakes are being enlarged by glacier retreat except Maud lake, which has been reduced in size since 1995 by the advance of Maud and Grey Glaciers.

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Thermal structure of proglacial lakes in Patagonia

et al. 2016

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Calving glaciers are rapidly retreating in many regions under the influence of ice‐water interactions at the glacier front. In contrast to the numerous researches conducted on fjords in front of tidewater glaciers, very few studies have been reported on lakes in which freshwater calving glaciers terminate. To better understand ice‐water interactions at the front of freshwater calving glaciers, we measured lakewater temperature, turbidity, and bathymetry near Glaciar Perito Moreno, Upsala, and Viedma, large calving glaciers of the Southern Patagonia Icefield. The thermal structures of these lakes were significantly different from those reported in glacial fjords. There was no indication of upwelling subglacial meltwater; instead, turbid and cold glacial water discharge filled the region near the lake bottom. This was because water density was controlled by suspended sediment concentrations rather than by water temperature. Near‐surface wind‐driven circulation reaches a depth of ~180 m, forming a relatively warm isothermal layer (mean temperature of ~5–6°C at Perito Moreno, ~3–4°C at Upsala, and ~6–7°C at Viedma), which should convey heat energy to the ice‐water interface. However, the deeper part of the glacier front is in contact with stratified cold water, implying a limited amount of melting there. In the lake in front of Glaciar Viedma, the region deeper than 120 m was filled entirely with turbid and very cold water at pressure melting temperature. Our results revealed a previously unexplored thermal structure of proglacial lakes in Patagonia, suggesting its importance in the subaqueous melting of freshwater calving glaciers.

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Downwasting of the Tasman Glacier, South Island, New Zealand: Changes in the terminus region between 1971 and 1993

Cited by 54 publications

References 29 publications

Co-registration and bias corrections of satellite elevation data sets for quantifying glacier thickness change

Co-registration and bias corrections of satellite elevation data sets for quantifying glacier thickness change

Temperature and bathymetry of ice‐contact lakes in Mount Cook National Park, New Zealand

Thermal structure of proglacial lakes in Patagonia

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