Ablation

Ablation readings were made at many stakes on both Nordbogletscher and Qamanârssûp sermia but the present paper refers only to measurements at stake 53 (at 880 m a.s.l.) on Nordbogletscher and at stake 751 (at 790 m a.s.l.) on Qamanârssûp sermia near the margins of the respective glaciers, i.e. about 200 m from the margin at Nordbogletscher and about 100 m at Qamanârssûp sermia. These were the so-called “daily stakes” which were measured almost every day in the late afternoon or early evening. The ablation “day” is not therefore identical to the reference period for daily climate data (see below).

The data mainly refer to ice ablation as both sites have little or no winter snow, although traces of new snow occur occasionally in cold periods during the summer (averages of 4 and 3 d/month at Nordbogletscher and Qamanârssûp sermia, respectively). Ice ablation is determined by measuring the lowering of the ice surface relative to the top of the stake and assuming a constant density for ice. The latter is not exactly correct as the density of the glacier-surface layer depends on weather conditions; a whitish “weathering crust” (Reference AmbachAmbach, 1963, p. 185–86: Reference Müller and KeelerMüller and Keeler, 1969) several centimetres deep often develops in sunny weather due to internal melting and disappears again under rainy or cloudy conditions. Although important on a short-term basis, these density variations have little effect on calculated ablation totals for longer periods.

The “daily stakes” at Qamanârssûp sermia, and at Nordbogletscher since 1981, are actually three separate stakes within a few metres of each other. Despite their closeness, the stakes seldom register the same ablation because of measurement errors and differences in micro-topography. The inter-stake difference has standard deviations of ±13 to ±19 mm water d⁻¹ for daily ablation (Reference BraithwaiteBraithwaite, 1985, p. 21–22).

Climate

The meteorological measurements at the field stations are made by simple recording instruments, supplemented by hand observations in the mornings and evenings. All data are analysed with respect to the day 0–24 h Greenland summer time (UCT minus 3 h).

Air temperature and relative humidity are recorded continuously by Lambrecht thermohygrographs in standard instrument shelters 2 m above ground. The vapour pressure of the air is calculated from air temperature and relative humidity (Reference WilsonWilson, 1974, p. 8). The run-of-wind is read twice-daily from Lambrecht cup anemometers mounted 4 m above the ground, and average wind speeds are calculated for 12 and 24 h intervals. Global radiation, i.e. short-wave radiation from sun and sky, is recorded with Belfort actinographs, supplemented by daily sunshine duration from Campbell-Stokes recorders. The actinographs were installed in 1981 and values for earlier periods, i.e. for 1979–80 at Nordbogletscher and for 1980 at Qamanârssûp sermia, are calculated from observed sunshine duration by an empirical equation (Appendix).

Climate data are available for longer periods than indicated by Table I which refers to availability of combined ablation and climate data. For example, climate measurements were made at Nordbogletscher in 1978 and June 1979 before daily ablation measurements were started in July 1979.

Albation

The simulated ablation ABL* is obtained from

(1)

where SHF and LHF are turbulent sensible- and latent-heat fluxes, and SWR and LWR are the short-wave and long-wave radiation fluxes. The observed ablation ABL is given by

(2)

where ERR accounts for errors in both the data and in the model, or caused by neglected terms, e.g. heat flux into the ice. As defined in Equation (2), ERR can be regarded as a fifth energy-balance component. For convenience, all the ablation sources are expressed in equivalent ablation units, i.e. as mm water d⁻¹ or kgm⁻²d⁻¹.

Turbulent-heat fluxes

Turbulent-heat fluxes are often described by flux-gradient relations where SHF and LHF are proportional to the vertical gradients of air temperature and absolute humidity in the air immediately over the glacier surface. The correct formulations of these relations are difficult but Reference AmbachAmbach (1986) has suggested simple approximations based upon energy-balance measurements on the Greenland ice sheet (Reference AmbachAmbach, 1963, 1977). These approximations are valid for a melting glacier surface, i.e. temperature equal to 0°C and vapour pressure equal to the saturation vapour pressure at 0°C, and assuming an adiabatic stratification in a Prandtl-type boundary layer with different aerodynamic roughness parameters for ice and snow surfaces. The suggested relations are

(3)

and

(4)

where K _S and K _L are coefficients, Ρ is atmospheric pressure, T ₂ is air temperature, V ₂ is wind speed, and Δe ₂ is the difference between vapour pressure of the air and saturation vapour pressure at the glacier surface. The subscript “2” indicates that temperature, wind speed, and vapour pressure are taken at 2 m above the glacier surface. A constant air pressure, depending only on elevation, is used for each station (91.3 and 92.4 kPa, respectively) as pressure variations due to different weather are small.

The numerical values of K _S and K _L are given in Table II in SI units for SHF and LHF in mm water d⁻¹, T ₂ in °C, V ₂ in m s⁻¹, and Δe ₂ and Ρ in Pa.

Table II.

Numerical Values Of Sensible- And Latent-Heat Flux Parameters (Reference AmbachAmbach, 1986)

The assumptions that sensible- and latent-heat fluxes are proportional to air temperature and vapour pressure, respectively, are similar to those made by Reference KuhnKuhn (1979),Reference Vetter Escher-Vetter (1985), and Reference Hay and FitzharrisHay and Fitzharris (1988). The heat-transfer coefficient of Kuhn, also used by Escher-Vetter, is approximately equal to K _S PV ₂ in present terminology. The bulk-exchange coefficient Κ of Reference Hay and FitzharrisHay and Fitzharris (1988) is proportional to Ambach’s K _S, parameter (Reference BraithwaiteBraithwaite, 1988)

Short-wave radiation

The short-wave radiation flux in mm water d⁻¹ is given by

(5)

where α is the albedo, G is the global radiation in MJm⁻²d⁻¹ and 0.335 MJ kg⁻¹ is the latent heat of fusion.Reference Ambach Ambach (1986) assumed the albedo α is 0.3 for ice and 0.7 for snow.

Long-wave radiation

The long-wave radiation flux in mm water d⁻¹ is given by

(6)

where , is the incoming long-wave radiation and 27.35 is the outgoing long-wave radiation from the melting glacier surface (both in MJ m⁻²d⁻¹ units). The incoming long-wave radiation is given by

(7)

where ε* is the effective emissivity of the sky, σ is the Stefan-Boltzmann constant, and T_a is the air temperature on the absolute scale. The effective emissivity ε* is expressed in terms of cloud cover n, and the emissivity of the clear sky ε₀ by

(8)

where k is a constant depending on cloud type. Reference OhmuraOhmura (1981, p. 243) listed k values for eight different cloud types but a constant value of 0.26 is assumed here (the average of Ohmura’s k values for A _c, A _a, S _c, and S _t cloud types). According to Reference OhmuraOhmura (1981, p. 229), the clear-sky emissivity is

(9)

where the temperature-dependence accounts for the increase of absolute humidity with temperature.

With present assumptions, the effective emissivity according to Equation (8) varies from 0.73 to 0.96 at both Nordbogletscher and Qamanârssûp sermia.

Surface conditions

The model takes account of differences between ice and snow surfaces, e.g. according to Table II sensible and latent fluxes to a snow surface are 30% lower than those to an ice surface under the same climatic conditions. The short-wave radiation flux is also 57% less for a snow surface (assumed albedo α = 0.7) than for an ice surface (α = 0.3) with the same global radiation.

The model assumes a melting glacier surface but there are days when the combined ablation sources are not strong enough to maintain the glacier surface at the melting point.

This usually occurs with air temperatures below zero but sometimes at positive temperatures as discussed by Reference KuhnKuhn (1987). The calculated ablation in these cases is re-set to zero in the model.

Daily and monthly ablation

On average, the simulations are surprisingly accurate considering the simplicity of the model. For example, the mean of the error ERR = ABL - ABL* is only −1.1 and −1.3 mm water d⁻¹ for Nordbogletscher (14 months) and Qamanârssûp sermia (21 months), respectively. However, errors are much bigger on a day-to-day basis, e.g. the standard deviation of ERR is ±13.6 and ±18.9 mm water d⁻¹ for the two cases, which means that errors account for 45 and 42%, respectively, of the day-to-day ablation variance.

Daily-averaged values of ablation and energy balance for different months are listed in Tables III and IV, respectively, while observed and simulated ablation rates are plotted against each other in Figure 2.

Fig. 2.

Observed and simulated ablation rates, (a) 14 months at Nordbogletscher; (b) 21 months at Qamanârssûp sermia.

Table III.

Ablation And Simulated Energy Balance For 14 months At Nordbogletscher. Units are mm water d⁻¹

*Global radiation estimated from sunshine duration.

Table IV.

Ablation And Simulated Energy Balance For 21 months AT Qamanârssûp Sermia. Units are mm water d⁻¹

The error ERR for daily-averaged ablation is much lower than for raw daily data, i.e. with standard deviations of ±3.0 and ±7.0 mm water d⁻¹ for Nordbogletscher and Qamanârssûp sermia, respectively. Apart from the greater amplitude of error at Qamanârssûp sermia, there appears to be a seasonal trend from negative errors in June to positive errors in August.

Errors

The errors in measuring ablation are an obvious source of the error ERR. For example, there is remarkable agreement between the standard deviations of ERR for daily data and the range of ±13 to ±19 mm water d⁻¹ quoted by Reference BraithwaiteBraithwaite (1985, p. 21–22) for this error in measuring daily ablation but measurement errors cannot be the only source of error. For example, the daily ablation and climate data are based on different definitions of “day”, although it is difficult to estimate the magnitude of error here.

Another cause of error is neglect of terms in the energy-balance model. The model does not include heat conducted into the ice as there are no data but this can be roughly assessed by analogy with other situations. For example, this heat flux amounted to −1.0 to −1.9 MJ m⁻²d⁻¹ for four series from Arctic Canada (Reference AmbachBraithwaite, 1981), which is equivalent to only −3 to −6 mm water d⁻¹ in ablation units. However, the active layer at both Nordbogletscher and Qamanârssûp sermia must be much warmer than in the Canadian cases, with lower englacial temperature gradients, so that heat conduction into the ice in the present cases is even smaller than in the Canadian cases. The heat provided by cooling of rainwater is also neglected in the model but a rough calculation shows that it is equivalent to less than 0.2 mm water d⁻¹ of ablation, which can be neglected.

Radiation errors

The error ERR has a negative correlation with SWR, i.e. r = −0.28 and r = −0.51 for Nordbogletscher and Qamanârssûp sermia, respectively, suggesting that errors in radiation are partly responsible for ERR. For example, albedo seems higher in sunny weather and lower in cloudy weather (according to subjective observation) due to formation of “ablation crust”. If true, this would give a negative correlation between ERR and SWR and, because SWR is highest in June, it would explain the apparent seasonal trend from negative to positive values of ERR. A trial re-calculation of the energy balance for Qamanârssûp sermia with an albedo of 0.4 for June (which is plausible) instead of 0.3 reduces the mean error for June ablation to only −2.4 compared with −8.1 mm water d⁻¹.

Another possibility is reduction in albedo from June to August due to increasing dirtiness of the glacier surface through the season (subjective observation). Routine measurements of albedo in future would help solve the problem.

Turbulent errors

Correlations between ERR and the turbulent fluxes SHF and LHF are not especially high but the model often underestimates ablation during Föhn events with high temperature and wind speed, and low humidity. This is curious as Reference AmbachAmbach (1963, p. 121) suggested that non-adiabatic stratification should reduce the tubulent fluxes by up to 12% compared with those calculated for the adiabatic assumption implicit in the model, i.e. the model should overestimate ablation under Föhn conditions. The underestimation found here may occur because we use daily means of climate data which might not accurately reflect the coincidence of high temperatures and wind speeds during Föhn. Although these events are fairly rare, they involve high ablation rates, i.e. 100–150 mm water d⁻¹, so it would be useful to improve the calculation of turbulent fluxes.

Sources of ablation energy

The importance of the various ablation sources varies from year to year and throughout the summer but the basic pattern is represented by the mean values at the two sites at the bottom of Tables III and IV, respectively.

The largest source of energy is short-wave radiation followed by sensible-heat flux and long-wave radiation. The latent-heat flux is very small on average but this is the result of substantial fluctuations between negative and positive daily fluxes, i.e. evaporation and condensation, respectively, which nearly cancel out over longer periods.

In conventional terms, radiation (SWR and LWR) accounts for about two-thirds of mean ablation at the two sites (73 and 69% at Nordbogletscher and Qamanârssûp sermia, respectively) and turbulence (SHF and LHF) accounts for one-third (31 and 34%, respectively). Errors only account for respectively −4 and −3% of mean monthly ablation. These relative contributions by radiation and turbulence agree quite well with the estimates byReference Braithwaite and Olesen Braithwaite and Olesen (1985) and with results of measurements by Reference Knudsen, Ottosen and SvendsenKnudsen and others (1987).

Differences between the two locations

The average ablation rate is higher at Qamanârssûp sermia than at Nordbogletscher because sensible-heat flux and short-wave radiation are both higher on average although slightly offset by lower latent-heat flux. This is because average temperature, wind speed, and global radiation are all generally higher at Qamanârssûp sermia (5.0 deg, 4.8 ms⁻¹, and 16.5 MJ m⁻²d⁻¹) than at Nordbogletscher (3.7 deg, 3.3 m s⁻¹, and 14.6 MJ m⁻²d⁻¹).

Ablation variations

Variations of ablation between different summers are illustrated by the deviations in Table V which refer to deviations of the summer averages from the means for four and seven summers, respectively.

Table V.

Summer Deviations Of Ablation And Energy Balance.Units Are mm water d⁻¹

Ablation at Nordbogletscher was low in summer 1983 mainly because of low short-wave radiation SWR (high cloudiness) but also due to low sensible-heat flux SHF (low temperature). Short-wave radiation was high in 1980 (low cloudiness) but this was nearly offset by low latent-heat flux (low humidity) and low long-wave radiation (low cloudiness), so the resulting average ablation was not exceptionally high in 1980.

Fig. 3.

Means of ablation and simulated energy balance for Nordbogletscher (14 months) and for Qamanârssûp sermia (21 months).

At Qamanârssûp sermia, the interpretation is more difficult because the amplitude of the error ERR is generally larger. For example, the error deviation in 1980 is larger than the ablation deviation, so the apparent low ablation in 1980 cannot be explained. However, there were clear cases of low ablation in 1983 and high ablation in 1985. The former was caused by low sensible-heat flux SHF (low temperature) and low short-wave radiation SWR (high cloudiness), while the high ablation in 1985 was due to high turbulent fluxes (high temperature and humidity) with short-wave radiation close to average.

Estimation Of Missing Data For Global Radiation

Following Reference WilsonWilson (1974, p. 39), global radiation is estimated from sunshine duration for days when measured data are missing according to the formula

(A1)

where G is the global radiation at the station, G₀ is the extra-terrestrial short-wave radiation, S is the observed sunshine duration, and S⁰ is the potential sunshine duration. The variables G₀ and S₀ depend upon latitude and are calculated for each day by equations in Reference SellersSellars (1965, p. 232)

The intercept a and the slope b in Equation (A1) are calculated by linear regression of observed G and S values for the days on which data are available for both. This gives a = 0.22 and b = 0.47 for Nordbogletscher (correlation coefficient r = 0.90 for 261 d), and a = 0.27 and b = 0.52 for Qamanârssûp sermia (r = 0.91 for 511 d). These a and b constants are not quite the same as given byReference Wilson Wilson (1974, p. 39) for middle latitudes.

Commenting on an early draft of this paper, Professor W. Ambach (personal communication) suggested that the a and b parameters might depend upon season.Reference Ambach Ambach (1963, p. 75) also gave a non-linear relation between G/G₀ and cloud amount. We therefore re-examined the validity of Equation (A1) by re-calculating the a and b parameters for each month separately. Although different values were found for different months, differences were not statistically significant at the 5% level. As a further check, the error in estimating global radiation from sunshine duration with constant a and b parameters was calculated for each month (Table VI) and was found to be small compared with the error ERR in the energy-balance calculation.

Table VI.

Errors In Calculating Global Radiation From Sunshine Duration. Units Are Mj m⁻²d⁻¹