Satellite-Derived Equilibrium Lines in Northern Patagonia Icefield, Chile, and Their Implications to Glacier Variations

Barcaza, Gonzalo; Aniya, Masamu; Matsumoto, Takane; Aoki, Takeshi

doi:10.1657/1938-4246-41.2.174

Cited by 35 publications

(29 citation statements)

References 32 publications

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“…Satellite data have been used to estimate the ELA by this approximation in remote regions and where mass balance is not measured (e.g. Barcaza et al, 2009;Jiskoot et al, 2009;Mathieu et al, 2009;Mernild et al, 2013;Rabatel et al, 2013;Shea et al, 2013). Since limited mass balance measurements exist for the outlet glaciers of this study (Fig.…”

Section: The Snowline Altitude Derived From Modis Imagery and The Lidmentioning

confidence: 99%

Changes in the southeast Vatnajökull ice cap, Iceland, between ~ 1890 and 2010

et al. 2015

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Abstract. Area and volume changes and the average geodetic mass balance of the non-surging outlet glaciers of the southeast Vatnajökull ice cap, Iceland, during different time periods between ∼ 1890 and 2010, are derived from a multi-temporal glacier inventory. A series of digital elevation models (DEMs) (∼ 1890, 1904, 1936, 1945, 1989, 2002, 2010) are compiled from glacial geomorphological features, historical photographs, maps, aerial images, DGPS measurements and a lidar survey. Given the mapped basal topography, we estimate volume changes since the end of the Little Ice Age (LIA) ∼ 1890. The variable volume loss of the outlets to similar climate forcing is related to their different hypsometry, basal topography, and the presence of proglacial lakes. In the post-LIA period, the glacierized area decreased by 164 km 2 (or from 1014 to 851 km 2 ) and the glaciers had lost 10-30 % of their ∼ 1890 area by 2010 (anywhere from 3 to 36 km 2 ). The glacier surface lowered by 150-270 m near the terminus and the outlet glaciers collectively lost 60 ± 8 km 3 of ice, which is equivalent to 0.15 ± 0.02 mm of sea-level rise. The volume loss of individual glaciers was in the range of 15-50 %, corresponding to a geodetic mass balance between −0.70 and −0.32 m w.e. a −1 . The annual rate of mass change during the post-LIA period was most negative in 2002-2010, on average −1.34 ± 0.12 m w.e. a −1 , which is among the most negative mass balance values recorded worldwide in the early 21st century.

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Section: The Snowline Altitude Derived From Modis Imagery and The Lidmentioning

confidence: 99%

Changes in the southeast Vatnajökull ice cap, Iceland, between ~ 1890 and 2010

et al. 2015

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“…The temperature records indicate a temperate climate, and the precipitation was distributed pretty evenly throughout year. Moderate air temperatures in winter implies some snow melting in the accumulation area even in winter and low air temperatures in summer implies snow fall in the accumulation area even in summer; therefore, accumulation and ablation occur almost year round (Barcaza et al, 2009).…”

Section: Hielo Patagónicomentioning

confidence: 99%

Holocene glaciations of Hielo Patag^|^oacute;nico (Patagonia Icefield), South America: A brief review

Aniya

2013

Geochem. J.

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“…The ice fields of Patagonia consist of alpine glaciers. The annual mass balances of both tidewater and nontidewater glaciers may be analyzed by equilibrium theory for small mountain glaciers [e.g., Naruse , 1997; Barcaza et al , 2009]. Classical mass balance analysis also applies to glaciers of the AP, but the strongest influence throughout the Antarctic Peninsula are ice shelf collapse events.…”

Section: Past Glacial Load Forcing and Gia Responsementioning

confidence: 99%

On-land ice loss and glacial isostatic adjustment at the Drake Passage: 2003–2009

Ivins¹,

Watkins²,

Yuan³

et al. 2011

J. Geophys. Res.

116

117

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Land glacier extent and volume at the northern and southern margins of the Drake Passage have been in a state of dramatic demise since the early 1990s. Here time‐varying space gravity observations from the Gravity Recovery and Climate Experiment (GRACE) are combined with Global Positioning System (GPS) bedrock uplift data to simultaneously solve for ice loss and for solid Earth glacial isostatic adjustment (GIA) to Little Ice Age (LIA) cryospheric loading. The present‐day ice loss rates are determined to be −26 ± 6 Gt/yr and −41.5 ± 9 Gt/yr in the Southern and Northern Patagonia Ice Fields (NPI+SPI) and Antarctic Peninsula (AP), respectively. These are consistent with estimates based upon thickness and flux changes. Bounds are recovered for elastic lithosphere thicknesses of 35 ≤ h ≤ 70 km and 20 ≤ h ≤ 45 km and for upper mantle viscosities of 4–8 × 1018 Pa s and 3–10 × 1019 Pa s (using a half‐space approximation) for NPI+SPI and AP, respectively, using an iterative forward model strategy. Antarctic Peninsula ice models with a prolonged LIA, extending to A.D. 1930, are favored in all χ2 fits to the GPS uplift data. This result is largely decoupled from Earth structure assumptions. The GIA corrections account for roughly 20–60% of the space‐determined secular gravity change. Collectively, the on‐land ice losses correspond to volume increases of the oceans equivalent to 0.19 ± 0.045 mm/yr of sea level rise for the last 15 years.

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Satellite-Derived Equilibrium Lines in Northern Patagonia Icefield, Chile, and Their Implications to Glacier Variations

Cited by 35 publications

References 32 publications

Changes in the southeast Vatnajökull ice cap, Iceland, between ~ 1890 and 2010

Changes in the southeast Vatnajökull ice cap, Iceland, between ~ 1890 and 2010

Holocene glaciations of Hielo Patag^|^oacute;nico (Patagonia Icefield), South America: A brief review

On-land ice loss and glacial isostatic adjustment at the Drake Passage: 2003–2009

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