Surface strain net

The NorthGRIP strain net was established between 1996 and 1999, and consisted of a total of 44 stakes plus a reference pole (Fig. 2).The reference pole was established in 1997, 500 mwest of the NorthGRIP drill site, by fixing a 102 maluminiumpole with a steel base into a 98.6m deep hole. the reference pole replaced a semi-deep (10 m) preliminary reference pole set up in 1996. Sixteen stakes were installed in 1996 in two concentric circles with radii of approximately 10 and 50 km, respectively, centred around the preliminary reference pole. In 1997, 16 stakes were installed in a strain net within 6–7km of the reference pole. In 1998, 12 stakes were installed in four groups of three, placed along the ridge with spacings of 10 km upstream from the reference pole, towards the GRIP site at Summit.

Fig. 2 Observed surface velocity at 44 stakes around the NorthGRIP site. Arrow length is scaled according to the measured surface velocity (scale in lower left corner), and the direction indicates flow direction. Stakes are marked by open squares. TheNorthGRIP reference pole (not marked) is located in the centre of stakes at position 75.10˚ N, 42.30˚W, and has a surface velocity of 1.329 ± 0.015 m a^–

The NorthGRIP deep-fixed reference pole was positioned with static GPS in 1997,1998,1999 and 2001. (The semi-deep preliminary reference pole was used in 1996.) Each year, several 24 hour sessions of GPS data were processed with the Bernese software in a network with four GPS reference stations (Thule, Kelly Ville (Kangerlussuaq/Sondrestrom), Reykjavík and Ny Ålesund; in 2001, Thule was replaced by the modernized GPS station, Thule 2, also located at Thule Air Base), using precise orbits and an ionospheric-free solution with float ambiguities. All processing was carried out in the appropriate time epoch, and after that, yearly solutions were transformed back to the International Terrestrial Reference Frame 94 (ITRF94) (epoch 15-08-1997) using Thule as the only fixed station. Thus, we were able to minimize geodynamic influence in our data. the movement observed between two years was corrected for the length of the measurement period in order to obtain the annual movement over 365 days. the observed positions and the derived annual surface movements at NorthGRIP are listed in Tables 1 and 2, respectively. the mean annual surface movement at NorthGRIP is 1.329 ±0.015 ma^–1 in the northwest direction. the observed mean change in height is consistent with the observed thickness of an annual layer at 100 m depth, 0.195 m (personal communication from H. B. Clausen, 2001)

GPS survey and results

Each year, the strain-net stakes were occupied using static GPS, organized into groups with local position periods of approximately 30 min for baselines up to 10 km, and of 1–3 hours for positioning stakes further away from the control site. Surface velocities of the stakes relative to the reference pole were determined from the repeated occupations (Fig. 3). Uncertainties in the relative velocity estimates depend on the precision of the repeated occupations and the GPS processing. Our estimates of the uncertainty range from 0.02m a^–1 for the very precise short baselines, to 0.30ma^–1 for the poorest-positioned stakes at distances of up to 80 km from the control site. the GPS datawere processed using standard processing softwareGPSurvey ver. 2.35 from Trimble, including precise orbit data and an ionospheric-free fixed or float solution. Surface velocities (Fig. 2) are perpendicular to the surface contour lines. They are almost constant along the ridge, and increase with distance from the ridge. the highest velocities are west of the ridge, where the surface slope increases.

Fig. 3 Surface velocity at the stakes relative to the reference pole (asterisk). Arrow length is scaled according to the measured relative surface velocity (scale in lower left corner), and the direction indicates direction of flow relative to the reference pole. Stakes are marked by open squares. for clarity, only data from 16 stakes are shown. These stakes are located in approximate circles around the reference pole with radii of 10 and 50 km.

Ice thickness

Airborne radar measurements of ice thickness in central and North Greenland have been compiled to give ice thickness along the north-northwest ridge from Summit to NorthGRIP (Reference Dahl-JensenDahl-Jensen and others, 1997) (Fig. 4). the bedrock is smooth in the strain-net area, with variations of <50m. the ice thickness at NorthGRIP is 3085 m with an accuracy of ±50m. Density measurements on the NorthGRIP core show a content of 25 mof air in the firn (personal communication from H.B. Clausen, 2001), giving an ice equivalent thickness of 3060m ice.

Fig. 4 Observed surface and bedrock topography along the flowline from Summit along the north-northwest ridge, passing the GRIP site (3 km from the topographic dome) and the NorthGRIP site (320 km from Summit). Data are compiled by Reference Dahl-JensenDahl-Jensen and others (1997).

Accumulation rate

The accumulation rate and vertical strain rate have been determined in the NorthGRIP core by identified volcanic reference horizons in the electrical conductivity record of the ice core. the accumulation rate between 1783 (the Laki (Iceland) volcanic eruption) and 1996 is 0.188 m ice equivalent a^–1, with an uncertainty of 0.005m ice equivalent a^–1 (personal communication from H. B. Clausen, 2001). Previously, the accumulation rate in North Greenland has been determined from shallow cores, and average rates over 4000 years have been derived from internal radio-echo layers along the north-northwest ridge (Reference Dahl-JensenDahl-Jensen and others, 1997). These data agree with the accumulation rate determined from the NorthGRIP ice core, and they consistently show that the accumulation rate has been unchanged over several thousand years.

Ice temperature

The mean annual surface temperature at NorthGRIP is –31.5˚C. the bottom temperature is not yet known, but preliminary logging of the drillhole points to a temperature close to the pressure-melting point of –2.4˚C (assuming a rate of change of melting point of –8.5610^–8 K Pa^–1 (Reference PatersonPaterson,1994, p.212) and an ice thickness of 3060 m ice equivalent) (Reference Dahl-JensenDahl-Jensen and others, 2002).

Principal surface strain rates

At the reference pole, horizontal principal surface strain rates are determined from the surface velocity data. This is done by calculating the radial strain rate for each stake, and determining the best-fit sine to the variation of the radial strain rates vs the direction to the stake from the reference pole. the principal strain rates are and (uncertainty given as twice the standard deviation). the principal axes are in directions y₁ = –15˚ from north, and y₂ = 75˚ from north, i.e. the first principal axis coincides with the direction of the ridge. the sum of the principal surface strain rates, balances (within the uncertainty) the average vertical strain rate in the upper part of the ice at NorthGRIP which is found to be based on a preliminary time-scale for the NorthGRIP ice core (Johnsen and others 2001; personal communication from S.J. Johnsen, 2001). the strain rate along the ridge is negative, and one order of magnitude smaller than the strain rate transverse to the ridge. This result shows that ice flows along the north-northwest ridge with an almost constant, but slightly decreasing velocity, i.e. the flow is slowed down as it moves along the ridge. the flow is divergent, and vertical compression is almost balanced by horizontal stretching transverse to the ridge, but there is a small horizontal compression along the ridge.

Mass balance

The local mass balance at NorthGRIP is estimated from the continuity equation, which combines observations of ice thickness, accumulation rate, surface velocity and strain rates at the NorthGRIP site. the vertical variation of horizontal velocity is modelled with an ice-flow model, which takes into account divergence of the flow.

We introduce a horizontal (x-y) coordinate system, with the x axis following the flowline in the direction of the flow. In this coordinate system, the continuity equation may be written (derived from Reference PatersonPaterson,1994, p.257)

where H is ice thickness (in m ice equivalent), t is time, b is the surface accumulation rate (in mice equivalent a^–1), b ' is the bottom melting (negative, in m ice equivalent a^–1), f is the velocity shape factor, defined as f = u_m/u_S, where u_m is the vertically averaged horizontal velocity, u_S is the horizontal surface velocity in the x direction, and is the sum of the horizontal principal surface strain rates. It is assumed that the velocity shape factor does not change along the flowline.

The vertical variation of the horizontal velocity is derived from an ice-flow model (Reference HvidbergHvidberg, 1996; Reference Hvidberg, Dahl-Jensen and WaddingtonHvidberg and others, 1997a). the model is based on Glen’s flow law, and simulates the thermomechanically coupled ice and heat flow along a flowline. the model includes longitudinal stresses, and takes into account divergence of the flow. Shear stresses transverse to the flowline are disregarded. It is assumed that the direction of the flow does not change with depth, that the flowline is perpendicular to the surface contour lines, and that divergence of the flow may be expressed in terms of the radius of curvature of surface contour lines at their intersection with the flowline. the model simulates the flow along a flowline departing from Summit and running along the north-northwest ridge. the flowline passes the GRIP and NorthGRIP sites (Fig. 1). the model is based on the topography data shown in Figure 4, and radii of curvature of surface contours along the flowline are derived from Figure 1. the velocity shape factor at NorthGRIP is calculated to be f = 0.88. This calculation assumes a bottom temperature close to the pressure-melting point, but no bottom sliding. the calculation of f is sensitive to the distribution of temperature with depth, in particular to the bottom conditions, which determine whether the ice is frozen to the bed or sliding. Assuming that bottom sliding accounts for 50% of the observed surface velocity, and the relative variation of velocity due to ice deformation is as above, the shape factor

would be 0.94. Based on this, we estimate the uncertainty of f to be 0.06 due to the unknown bottom conditions. the shape

factor is also affected by changes in longitudinal stresses (stretching or compression) along the flowline (discussed by, e.g., Reference ReehReeh 1988). Bedrock topography or changes in the divergence of the flow would introduce longitudinal stress gradients. Along the north-northwest ridge at NorthGRIP, however, the divergence is constant, the horizontal surface velocity is almost constant, the surface slope is constant, and the bedrock is almost horizontal. Therefore, we neglect a possible contribution to the uncertainty of f from longitudinal stress gradients.

The mass balance of the Greenland ice sheet at NorthGRIP is now estimated from the continuity equation (1) by applying the following values: H =3060±50mice equivalent, b 0.188= ±0.005m ice equivalent a^–1, b0 =–0.002 ±0.002m ice equivalent a^–1, uS = 1.329±0.015ma^–1, (͘ε₁ ͘ε₂) + = (6.6±= –0.7610^–3, and f = 0.9)610^–5 a^–1, ∂H/∂x 0.94 ±0.06. the result is:

assuming sliding accounts for 50% of the ice movement, and a bottom melting of 2mma^–1, as suggested by analysis of ice-core data (Reference Grinsted and Dahl-JensenGrinsted and Dahl-Jensen, 2002). If ice is frozen to the bed with no sliding or melting, f = 0.88 and b' = 0, the result is ∂H/∂t = 0.01 ±0.04ma^–1. the uncertainty of ∂H/∂t is dominated by the uncertainty of the surface strain rates and the uncertainty of f.

Strain rates: implications for stratigraphy at NorthGRIP

Surface strain rates contribute to knowledge of the flow and may be used to constrain ice-flow models. the flow pattern at NorthGRIP is complicated for several reasons: (1) ice flow along the north-northwest ridge is highly divergent; (2) bottom melting may occur at NorthGRIP or upstream along the ridge as suggested by preliminary ice-core measurements (Reference Dahl-JensenDahl-Jensen and others, 2002; Reference Grinsted and Dahl-JensenGrinsted and Dahl-Jensen, 2002) and analysis of internal radio-echo layers (Reference Dahl-JensenDahl-Jensen and others, 1997); and (3) the bottom temperature at NorthGRIP is expected to be close to the pressure-melting point based on preliminary temperature logging in the borehole down to 80 m above the bed (Reference Dahl-JensenDahl-Jensen and others, 2002). Below, we use strain-rate data to discuss the influence of these complications on the stratigraphy at NorthGRIP.

In a previous survey, surface velocities were measured around Summit (Reference Hvidberg, Keller, Gundestrup, Tscherning and ForsbergHvidberg and others, 1997b). the GRIP site was found to be 3 km from the topographic dome, with a surface velocity of 0.25 ±0.06 ma^–1 in the northwest direction. At a stake located 33.4 km from GRIP in the direction of the flowline between GRIP and NorthGRIP, the surface velocity was measured to be 1.62±0.11ma^–1 in the northwest direction. the average compressive strain rate along the ridge between this stake and NorthGRIP is –1.0610^–6 a^–1. This is lower in magnitude than the strain rate observed at NorthGRIP, and the data imply that the horizontal surface velocity must reach a maximum between the two positions. A simple calculation assuming axial-symmetrical flow within 125 km of Summit (this is realistic according to the description in the ``Region of study’’ section above), an average accumulation rate of 0.20m ice equivalent a<sup>–1</sup> (Reference Dahl-JensenDahl-Jensen and others, 1997) and an ice thickness of 3000 myields a depth-averaged horizontal velocity of 4.2ma<sup>–1</sup> 125 km from Summit. At a distance of about 150 km from Summit (73.5–74˚ N), the divergence of the flow increases, and the flow is probably slowed down rapidly as the flowline passes the transition to the north-northwest ridge, where the surface slope is small. from a distance of about 200 km from Summit (74–74.5˚N), the divergence remains constant along the flowline until north of NorthGRIP. A rapid reduction in the ice-flow rate at 150–200km from Summit implies enhanced stretching transverse to the ridge, with unknown implications for the layer stratigraphy. A preliminary result of our modelling is that the shape factor of the horizontal velocity increases at 150–200km from Summit as a result of the increased divergence in that area, which also causes the bottom temperatures to increase (the model is described in ``Mass balance’’ in the previous section). This implies enhanced ice deformation in the bottom layers, which is expected to cause annual layers to be dragged down in this region. Reference Dahl-JensenDahl-Jensen and others (1997) compared observed radar reflection layers with modelled annual layers. Their model did not take into account effects from divergence of the flow, and at 150–200km from GRIP the observed internal layers stacked up to 200m deeper in the ice than the layers predicted by their model. This is within the area with increased divergence. They attributed the dip of the observed layers to bottom melting. Bottom melting would also drag annual layers down. the flow pattern in the region with increased divergence affects the downstream stratigraphy. If we assume that ice moves with a constant surface velocity as observed at NorthGRIP, a rough estimate is that at NorthGRIP, which is 120–170 km downstream, ice older than 90 000 years is affected so that it exhibits thicker annual layers than expected from the local flow pattern. This could contribute to making the deep ice younger than expected in the NorthGRIP core (Reference Dahl-JensenDahl-Jensen and others, 2002).

Mass balance: our result confirms previous estimates

The method used to determine the mass balance has been applied to other locations on the Greenland ice sheet (e.g. Reference Reeh and GundestrupReeh and Gundestrup, 1985; Reference Hvidberg, Keller, Gundestrup, Tscherning and ForsbergHvidberg and others, 1997b). the method requires accurate surface velocity and strain-rate data. At NorthGRIP, the uncertainty of the velocity is 1%, but the sum of the surface strain rates has an uncertainty of 14%. Our calculation of principal strain rates does not take into account that the ridge is not ideally symmetrical over the strain-net area, and that the ridge could be migrating at present. These effects may contribute to the uncertainty of the strain rates. It is not possible, however, to analyze the data for the stability of the ridge before the bottom conditions are known, thereby providing better constraints on the vertical distribution of horizontal velocity.

Our result shows that the Greenland ice sheet is close to mass balance at NorthGRIP. the result confirms other estimates of ice-thickness change. Repeated airborne laser-altimeter surveys over the Greenland ice sheet yield an average thickening rate between 1994 and 1999 of <0.010ma^–1 in the high-elevation areas north of 70˚N (Reference KrabillKrabill and others, 2000). Comparison of ice flux across the 2000 m contour line with the total snow accumulation within this perimeter has been used to estimate the ice-thickening rates over the past few decades in regions in the high-elevation area of the Greenland ice sheet (Reference ThomasThomas and others, 2000). In that study, the region west of the ridge at NorthGRIP has an average thickening rate of –0.051±0.017ma^–1, while the area east of the ridge has an average thickening rate of +0.021±0.006ma^–1. This is consistent with our result of NorthGRIP being close to steady state.