Surface energy balance, parameterizations of boundary-layer heights and the application of resistance laws near an Antarctic Ice Shelf front

Heinemann, Günther; Rose, L.A.

doi:10.1007/bf00120464

Cited by 47 publications

(19 citation statements)

References 47 publications

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“…In spite of this, results from numerous dedicated off-pole meteorological experiments show a strong diurnal cycle of summertime Antarctic surface-layer climate and SEB (Liljequist, 1957;Ohata et al, 1985;Wendler et al, 1988;Heinemann and Rose, 1990; Van den Broeke and Bintanja, 1995;Bintanja and van den Broeke, 1995;Mastrantonio et al, 1999;Bintanja, 2000;Van As et al, 2005a;Argentini et al, 2005;King et al, 2006). Similar results have been reported on the basis of data from automatic weather stations (AWS, Kikuchi et al, 1988;Allison, 1985;Clow et al, 1988;Stearns and Weidner, 1993;Reijmer and Oerlemans, 2002;Renfrew and Anderson, 2002), as well as theoretical and numerical modelling studies (Gallée and Schayes, 1992;Parish et al, 1993;Sorbjan et al, 1986;.…”

Section: Introductionsupporting

confidence: 52%

Daily cycle of the surface energy balance in Antarctica and the influence of clouds

Broeke

Reijmer

et al. 2006

Intl Journal of Climatology

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We present the summertime daily cycle of the Antarctic surface energy balance (SEB) and its sensitivity to cloud cover. We use data of automatic weather stations (AWS) located in four major Antarctic climate zones: the coastal ice shelf, the coastal and interior katabatic wind zone and the interior plateau. Absorbed short wave radiation drives the daily cycle of the SEB, in spite of the high surface albedo (0.84-0.88). The dominant heat sink is the cooling by long wave radiation, but this flux is distributed more evenly throughout the day so that a pronounced daily cycle in net all-wave radiation remains with all-sky night-time heat losses of 20-30 W m −2 and noontime heat gains of 30-40 W m −2 . During the night, heat is re-supplied to the snow surface by the sensible heat flux, especially in the katabatic wind zone, and the sub-surface heat flux. Daytime radiative energy excess is removed from the surface by sublimation (except at the high plateau) and sub-surface heat transport. Daytime convection occurs at all sites around solar noon but is generally weak. Spatial differences in the SEB are largely controlled by differences in cloud cover. Clouds are associated with higher surface temperatures and near-surface wind speeds. This especially limits nocturnal cooling, so that the strongest daytime convection is found during overcast conditions on the interior plateau.

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Section: Introductionsupporting

confidence: 52%

Daily cycle of the surface energy balance in Antarctica and the influence of clouds

Broeke

Reijmer

et al. 2006

Intl Journal of Climatology

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“…The former is mainly of concern during the late autumn and early spring period when polar night conditions are absent, while the latter circumstance is unavoidable throughout each winter when relying on optical and infrared remote sensing data. Since lowlevel clouds reduce the net radiative loss by about 50 W m −2 in polar regions (Heinemann and Rose, 1990;König-Langlo and Augstein, 1994), the restriction to cloud-free conditions in the daily composites results in a positive bias in IP. Considering an average clear-sky fraction of 73 ± 8 % per pixel from all input swaths in a given daily composite and assuming that not all clouds are low level, the overestimation of net energy loss by our method can be estimated to be less than 10 W m −2 , which corresponds to less than 0.4 m IP per winter.…”

Section: Derivation Of Ice Production and Polynya Areamentioning

confidence: 99%

Circumpolar polynya regions and ice production in the Arctic: results from MODIS thermal infrared imagery from 2002/2003 to 2014/2015 with a regional focus on the Laptev Sea

et al. 2016

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Abstract. High-resolution MODIS thermal infrared satellite data are used to infer spatial and temporal characteristics of 17 prominent coastal polynya regions over the entire Arctic basin. Thin-ice thickness (TIT) distributions ( ≤ 20 cm) are calculated from MODIS ice-surface temperatures, combined with ECMWF ERA-Interim atmospheric reanalysis data in an energy balance model for 13 winter seasons (2002/2003to 2014/2015 November to March). From all available MODIS swath data, daily thin-ice thickness composites are computed in order to derive quantities such as polynya area and total thermodynamic (i.e., potential) ice production. A gap-filling approach is applied to account for cloud and data gaps in the MODIS composites. All polynya regions combined cover an average thin-ice area of 226.6 ± 36.1 × 10 3 km 2 in winter. This allows for an average total winter-accumulated ice production of about 1811 ± 293 km 3 , whereby the Kara Sea region, the North Water polynya (both 15 %), polynyas on the western side of Novaya Zemlya (20 %), as well as scattered smaller polynyas in the Canadian Arctic Archipelago (all combined 12 %) are the main contributors. Other wellknown sites of polynya formation (Laptev Sea, Chukchi Sea) show smaller contributions and range between 2 and 5 %. We notice distinct differences to earlier studies on pan-Arctic polynya characteristics, originating in some part from the use of high-resolution MODIS data, as the capability to resolve small-scale (> 2 km) polynyas and also large leads are increased. Despite the short record of 13 winter seasons, positive trends in ice production are detected for several regions of the eastern Arctic (most significantly in the Laptev Sea region with an increase of 6.8 km 3 yr −1 ) and the North Water polynya, while other polynyas in the western Arctic show a more pronounced variability with varying trends. We emphasize the role of the Laptev Sea polynyas as being a major influence on Transpolar Drift characteristics through a distinct relation between increasing ice production and ice area export. Overall, our study presents a spatially highly accurate characterization of circumpolar polynya dynamics and ice production, which should be valuable for future modeling efforts of atmosphere-ice-ocean interactions in the Arctic.

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“…Most Antarctic meteorological experiments dedicated to quantify SEB components have been summer-only type (Wendler et al, 1988;Heinemann and Rose, 1990;Bintanja and van den Broeke, 1995;Bintanja, 2000;van As et al, 2005a). Only a few experiments have covered the entire annual cycle (Liljequist, 1957;Carroll, 1982;Ohata et al, 1985;King et al, 1996), and these were often undertaken close to manned stations for reasons of power supply and sensor maintenance.…”

Section: Introductionmentioning

confidence: 99%

Sensible heat exchange at the Antarctic snow surface: a study with automatic weather stations

Broeke

Reijmer

et al. 2005

Intl Journal of Climatology

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Data of four automatic weather stations (AWSs) are used to calculate the turbulent exchange of sensible heat at the Antarctic snow surface for a 4 year period (1998)(1999)(2000)(2001). The AWSs are situated on the ice shelf, in the coastal/inland katabatic wind zone and on the interior plateau in Dronning Maud Land, East Antarctica. Sensible heat flux (SHF) is calculated using the aerodynamic 'bulk' method between a single AWS sensor level and the surface, in combination with surface temperature derived from upwelling longwave radiation and surface roughness derived from eddy correlation measurements. Good agreement is found between calculated and directly measured SHF. All AWS sites show a downwarddirected average sensible heat transport, but otherwise the differences between the various zones are large. The surface roughness for momentum differs by an order of magnitude between the interior plateau (0.02 mm) and the katabatic wind zone (0.16 mm). On the ice shelf, frequent clouds limit surface cooling, and annual mean SHF is small (8 W m −2 ). In contrast, clear skies prevail on the interior plateau, but weak winds, an aerodynamically smooth surface and stability effects limit annual mean SHF to an equally low value (8 W m −2 ). The most favourable conditions for sensible heat exchange are found in the katabatic wind zone, where a combination of strong winds, relatively little cloud cover and a rougher surface results in annual mean SHF values of 22 to 24 W m −2 .

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Surface energy balance, parameterizations of boundary-layer heights and the application of resistance laws near an Antarctic Ice Shelf front

Cited by 47 publications

References 47 publications

Daily cycle of the surface energy balance in Antarctica and the influence of clouds

Daily cycle of the surface energy balance in Antarctica and the influence of clouds

Circumpolar polynya regions and ice production in the Arctic: results from MODIS thermal infrared imagery from 2002/2003 to 2014/2015 with a regional focus on the Laptev Sea

Sensible heat exchange at the Antarctic snow surface: a study with automatic weather stations

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