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A laboratory study of particle ploughing and pore-pressure feedback: a velocity-weakening mechanism for soft glacier beds

Published online by Cambridge University Press:  08 September 2017

Jason F. Thomason and
Neal R. Iverson
Jason F. Thomason
Affiliation:
Department of Geological and Atmospheric Sciences, Iowa State University, Ames, Iowa 50011, USA E-mail: thomason@isgs.uiuc.edu
Neal R. Iverson
Affiliation:
Department of Geological and Atmospheric Sciences, Iowa State University, Ames, Iowa 50011, USA E-mail: thomason@isgs.uiuc.edu
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Abstract

If basal-water discharge and pressure are sufficiently high, a soft-bedded glacier will slip over its bed by ploughing, the process in which particles that span the ice–bed interface are dragged across the bed surface. Results of laboratory experiments indicate that resistance to ploughing can decrease with increasing ploughing velocity (velocity weakening). During ploughing at various velocities (15–400 m a−1), till was compacted in front of idealized particles, causing pore pressures there that were orders of magnitude higher than the ambient value. This excess pore pressure locally weakened the till in shear, thereby decreasing ploughing resistance by a factor of 3.0–6.6 with a six-fold increase in ploughing velocity. Characteristic timescales of pore-pressure diffusion and compaction down-glacier from ploughing particles depend on till diffusivity, ploughing velocity and sizes of ploughing particles. These timescales accurately predict the ranges of these variables over which excess pore pressure and velocity weakening occurred. Existing ploughing models do not account for velocity weakening. A new ploughing model with no adjustable parameters predicts ploughing resistance to no worse than 38% but requires that excess pore pressures be measured. Velocity weakening by this mechanism may affect fast glacier flow, sediment transport by bed deformation and basal seismicity.

Information

Type
Research Article
Information
Journal of Glaciology , Volume 54 , Issue 184 , 2008, pp. 169 - 181
Copyright
Copyright © International Glaciological Society 2008

1. Introduction

Resistance to basal movement of glaciers is usually thought to increase with slip velocity. This idea follows from classical sliding theories (Reference WeertmanWeertman, 1964; Reference NyeNye, 1969; Reference KambKamb, 1970; Reference FowlerFowler, 1981) and is consistent with the widely applied empirical rule, u = kτpN −q , where k, p and q are positive constants, u is sliding velocity, τ is basal shear stress and N is effective pressure (the ice-overburden pressure minus the basal-water pressure (Reference PatersonPaterson, 1994)). However, for the case of a hard bed, Reference SchoofSchoof (2004) has extended the analysis of Reference FowlerFowler (1986) to show that, for randomly periodic bed roughness, slip resistance can decrease with increasing slip velocity, due to cavity growth in the lee of undulations and the resultant drowning of roughness elements. Decreasing slip resistance with increasing velocity is commonly called velocity weakening (e.g. Reference ScholzScholz, 2002, p. 83). During speedup of glaciers, it can focus the downslope component of glacier weight on parts of the bed not subject to velocity weakening or on the glacier sides, thereby contributing to further increases in speed.

Thus, an important question is whether soft beds, which are thought to more readily promote fast glacier flow and sediment mobilization (Reference ClarkeClarke, 2005), are also susceptible to velocity weakening. Laboratory experiments indicate that till, probably the most common subglacial sediment, exhibits Coulomb–plastic behavior, such that its strength is independent of deformation rate and linearly dependent on effective normal stress (Reference KambKamb, 1991; Reference Iverson, Hooyer and BakerIverson and others, 1998; Reference Tulaczyk, Kamb and EngelhardtTulaczyk and others, 2000). Minor velocity weakening was exhibited in the study of Reference Iverson, Hooyer and BakerIverson and others (1998), in which steady-state shear strength of two basal tills decreased by ∼1% per 100 m a−1 increase in shear velocity. This is a small effect, however, and the observation that some tills, rather than weakening, strengthen by similarly small amounts with increasing deformation rate (e.g. Reference Tika, Vaughan and LemosTika and others, 1996; Reference TulaczykTulaczyk, 2006) indicates that velocity weakening is not an intrinsic property of till.

Glaciers can also move over a soft bed by ploughing, the process in which particles embedded partway in the glacier sole are dragged across the bed surface (Reference Brown, Hallet and BoothBrown and others, 1987; Reference AlleyAlley, 1989; Reference IversonIverson, 1999; Reference Tulaczyk, Mickelson and AttigTulaczyk, 1999; Reference Iverson and HooyerIverson and Hooyer, 2004). During this slip process the bed deforms locally near its surface in the vicinity of ploughing particles. The tendency for basal motion to be focused at or near the surfaces of soft beds when basal-water pressure is rising or high has been demonstrated in studies at a number of modern glaciers (Reference Blake, Fischer and ClarkeBlake and others, 1994; Reference Iverson, Hanson, Hooke and JanssonIverson and others, 1995, Reference Iverson2003, Reference Iverson2007; Reference Engelhardt and KambEngelhardt and Kamb, 1998; Reference Truffer and HarrisonTruffer and Harrison, 2006). Ploughing is the most likely mechanism for this movement. When basal-water discharge and pressure are high, the water layer at the bed surface thickens, focusing shear stresses on fewer particles and increasing their likelihood of ploughing through the till bed, which is weakened by high pore pressure (Reference IversonIverson, 1999; Reference IversonIverson and others, 2007). Evidence of particle ploughing is common in the geological record from past and modern glacial environments (Fig. 1) (e.g. Reference Clark and HanselClark and Hansel, 1989; Reference KrzyszkowskiKrzyszkowski, 1994; Reference Jørgensen and PiotrowskiJørgensen and Piotrowski, 2003; Christofferson and others, 2005; Reference Piotrowski, Larsen, Menzies and WysotaPiotrowski and others, 2006), and the size distribution of particles that have ploughed has been used to estimate the sliding speed of a past ice sheet (Reference Iverson and HooyerIverson and Hooyer, 2004).

Fig. 1.

(a) Ploughing particles at the ice–till interface. (b) Cobble-sized clast (ruler is 0.3 m long) that has ploughed from left to right through Illinoian glacial sediments in central Illinois, leaving a groove up-glacier and a prow down-glacier (Reference Iverson and HooyerIverson and Hooyer, 2004). (c) More evidence of ploughing (from upper right to lower left) at the same location.

In this paper, we propose a velocity-weakening process associated with ploughing and test our hypothesis by pushing idealized particles through till with a large ring-shear device. A pore-pressure feedback is demonstrated that reduces ploughing resistance as ploughing velocity increases in some tills. The data also highlight weaknesses of existing mechanical models of particle ploughing (Reference Brown, Hallet and BoothBrown and others, 1987; Reference AlleyAlley, 1989; Reference IversonIverson, 1999; Reference Tulaczyk, Mickelson and AttigTulaczyk 1999) and provide the basis for a new model that incorporates pore-pressure feedback. This velocity-weakening mechanism could potentially promote fast glacier flow, focus motion at the bed surface and thereby inhibit pervasive bed deformation, and induce basal seismicity (e.g. Reference Anandakrishnan and BentleyAnandakrishnan and Bentley, 1993). The results are also relevant to ploughing on much larger scales: for example, ploughing by decameter-scale ice ‘keels’ on the bases of ice streams that may be responsible for submarine megalineations in glacier forefields (Reference Tulaczyk, Scherer and ClarkTulaczyk and others, 2001; Reference Clark, Tulaczyk, Stokes and CanalsClark and others, 2003).

2. Hypothesis: Velocity Weakening by Ploughing

Particles at the glacier sole that protrude partway into the substrate provide the roughness that couples a wet-based glacier to a soft bed. Slip at this interface requires some combination of ice movement past these particles by the classical sliding mechanisms (regelation and enhanced creep) and movement of the particles through the bed by ploughing. Clay, silt and fine sand particles at the bed surface that commonly constitute a large fraction of till will tend to be drowned in a water layer at the bed surface (Reference Brown, Hallet and BoothBrown and others, 1987; Reference AlleyAlley, 1989; Reference IversonIverson 1999; Reference Tulaczyk, Mickelson and AttigTulaczyk, 1999). Thus, for typical till grain-size distributions the real area of contact between ice and larger particles at the bed surface is a small fraction of the bed area (Reference AlleyAlley, 1989; Reference IversonIverson, 1999), so shear stresses are focused on larger particles. When pore-water pressure is high, these particles plough due to the low strength of the till. Thus, resistance to basal motion, averaged over the surface of the till bed, can be limited by ploughing and can be too small to shear the bed at depth or result in much movement by the classical sliding mechanisms (Reference Brown, Hallet and BoothBrown and others, 1987; Reference IversonIverson, 1999). Also, if ice penetrates the till bed by regelation infiltration (e.g. Reference ClarkeClarke, 2005), as has been observed in field experiments (Reference IversonIverson and others, 2007), then grain-to-grain friction in the resultant debris-charged ice will inhibit movement of this ice over the soft bed by the classical sliding mechanisms. Thus, basal movement due to yielding of the till bed associated with ploughing is even more likely in this case than when debris in ice is sparse.

Consider particles of different sizes ploughing through the surface of a water-saturated till bed (Fig. 1a). Till that is down-glacier from ploughing particles is compacted and sheared as particles move through it. Porosity reduction during compaction increases the pressure on till pore-water. The low hydraulic permeability of many tills requires that this increase in pore pressure be large in order to generate the hydraulic gradient necessary to drive water out of the compacted zone at the rate that pores are shrinking. As first noted by Reference Iverson, Jansson and HookeIverson and others (1994), the pore pressure in excess of the ambient pore pressure (hereinafter called the ‘excess’ pore pressure) should reduce effective stress in the bed down-glacier from ploughing objects, thereby reducing the till shear strength and the overall resistance to ploughing. Excess pore pressures are expected to increase with slip velocity, which will increase the ploughing speed and the rate of till compaction. Thus, as slip velocity increases, ploughing resistance will decrease. The magnitudes of excess pore pressure and velocity weakening will depend on the extent to which the rate of till compaction exceeds that of pore-pressure diffusion (Reference Iverson, Jansson and HookeIverson and others, 1994; Reference IversonIverson, 1999).

This velocity-weakening hypothesis is supported by field geotechnical studies in which an instrumented cone is pushed downward at constant speeds through water-saturated sediments. The resistance to movement of the cone decreases with both increasing penetration speed (Reference Finke, Mayne and KloppFinke and others, 2001) and decreasing hydraulic permeability (Reference Campanella, Robertson and GillespieCampanella and others, 1983). Pore-pressure measurements made adjacent to the cone demonstrate that these effects are due partly to excess pore pressures that weaken the sediment and decrease penetration resistance.

Some subglacial measurements are also consistent with this hypothesis. Reference Rousselot and FischerRousselot and Fischer (2005) drove a steel rod, through a borehole, into subglacial till at Unteraargletscher, Switzerland, which ploughed through the till during sliding. The rod contained a sensor that recorded the till pore pressure down-glacier from the rod. Water-pressure fluctuations in the borehole and in the till were strongly correlated, but those in the till were systematically higher in amplitude. The authors argued that the higher amplitude was likely to be due to increased sliding speed, that caused more rapid till compaction down-glacier from the rod during periods of high basal-water pressure. Earlier measurements of the force on a ploughing rod at Unteraargletscher also indicated that ploughing resistance may have been reduced by excess pore pressures correlated to increases in glacier velocity (Reference Fischer, Porter, Schuler, Evans and GudmundssonFischer and others, 2001).

3. Methods

Our aim was to study particle ploughing through till in the laboratory, measuring both pore pressure and ploughing resistance as a function of ploughing speed.

3.1. Apparatus

Our ring-shear device (Reference Iverson, Baker and HooyerIverson and others, 1997) shears a remolded-till specimen to high strains under effective normal stresses similar to those beneath soft-bedded glaciers (Fig. 2a). This device has been used to study the mechanical properties of various tills (Reference Iverson, Hooyer and BakerIverson and others, 1998; Reference Moore and IversonMoore and Iverson, 2002), particle alignment with strain (Reference Hooyer and IversonHooyer and Iverson, 2000a; Reference Thomason and IversonThomason and Iverson, 2006), mixing of granular materials in shear (Reference Hooyer and IversonHooyer and Iverson, 2000b) and particle comminution (Reference Iverson, Hooyer and HookeIverson and others, 1996; Reference Scherer, Sjunneskog, Iverson and HooyerScherer and others, 2004). The specimen occupies an annular chamber that has an outside diameter of 0.6 m and a width of 0.115 m, with a maximum specimen thickness of 0.08 m. The water-saturated till specimen is hydraulically connected to an internal water reservoir exposed to the atmosphere, so water can move to and from the till if its volume changes. A normal stress is applied to the sediment by a lever arm with dead weights that presses down on a thick aluminum load plate. This plate is fixed rotationally but is free to move vertically if the specimen thins or thickens. The upper walls do not rotate and press against the rotating lower walls to minimize loss of specimen volume. Shearing displacement occurs along an O-ring that separates the upper and lower walls. An electric motor drives two gearboxes that turn the bottom platen at a constant speed.

Fig. 2.

(a) Cross-section of the ring-shear device, as adapted for ploughing experiments. Dark gray components rotate. (b) Detail of the specimen chamber with insert that contains the hemispheres. (c) Specimen chamber with only the large hemisphere visible at left.

The device was adapted to push ploughing clasts, idealized as hemispheres (19.0 and 40.0 mm in diameter), through water-saturated till to large displacements. The hemispheres extended above an aluminum insert that occupied the lower part of the specimen chamber and moved with the rotating base (Fig. 2b and c). The surfaces of the hemispheres and insert were armored with a Teflon hard coat. Cylindrical extensions of the hemispheres were contained within the insert and rested on bearings (Fig. 3). Load cells within the insert recorded the bed-parallel forces exerted on the hemispheres in the direction opposite to that of ploughing. There were also pore-pressure sensors in the insert: two in front of and one behind each hemisphere. Water could escape from the till through the upper platen, which contains hundreds of 0.5 mm holes that connect to the internal water reservoir. A load cell located in the upper platen was used in some experiments to measure local stresses against the normal load plate as a hemisphere moved beneath it. This load cell recorded the force on a circular platen, 18 mm in diameter, which was mounted flush with the lower surface of the upper platen (Fig. 3).

Fig. 3.

Longitudinal cross-section of the specimen chamber in the vicinity of the large hemisphere. Movement direction of the hemisphere and adjacent insert is from left to right. The upper platen is fixed rotationally but can move up and down.

The load cells that recorded the horizontal force on the hemispheres were calibrated in situ. This was necessary to account for friction in the bearings and compression of O-rings between the hemisphere and the aluminum panel (Fig. 3), both of which supported some of the load exerted on the hemispheres by till. A cable was anchored to the hemisphere halfway up its face and was pulled under forces ranging from 0 to 200 N. A downward force commensurate with a normal stress of 65 kPa, equal to the normal stress applied to the till during experiments, was applied to the hemispheres during calibrations. Calibration regressions were linear, with coefficients of determination (R 2) greater than 0.98.

3.2. Procedure

Six experiments were performed with each of two tills: a fine-grained basal till of the Des Moines Lobe (Alden Member) and a coarse-grained till from an end moraine of Engabreen, a valley glacier in Norway. These tills were chosen due to their contrasting grain-size distributions and hydraulic diffusivities (Table 1). When till is compressed in front of a ploughing clast, excess pore-pressure generation depends on the hydraulic diffusivity of the till (Reference Freeze and CherryFreeze and Cherry, 1979, p.61), also called the coefficient of consolidation (Reference Lambe and WhitmanLambe and Whitman, 1969, p.407), which is proportional to the ratio of permeability to compressibility and is related to the grain-size distribution. Owing to its higher silt and clay fraction (Table 1), the Des Moines Lobe till is about 40 times less diffusive than the Engabreen till.

Table 1.

Till properties and experimental conditions

All particles >5 mm in diameter (10% of the smallest dimension of the sample chamber) were removed in accordance with standard geotechnical testing procedures (Reference HeadHead, 1989, p.83). These particles, due to their scarcity (less than 5% of the till volume was removed), would have tended to have been surrounded by finer particles, so the effect of removing these large particles on either the till’s internal friction or its permeability was probably small. This inference agrees with experience in geotechnical engineering that the fine fraction of poorly sorted sediments is primarily responsible for both their mechanical behavior (Reference Mitchell and SogaMitchell and Soga, 2005, p.432) and permeability (Reference Mitchell and SogaMitchell and Soga, 2005, p.256).

Remolded-till specimens were saturated with distilled water and added to the specimen chamber of the ring-shear device as a slurry. Prior to an experiment, the specimens were consolidated by applying a normal stress of 65 kPa to the normal-load plate with the lever arm and dead weights. Consolidation was complete when excess pore pressure dissipated and specimen thinning had effectively ceased. The reduction in consolidation rate with time was used to determine hydraulic diffusivity using the square-root-of-time method (Reference DasDas, 1998, p.340) (Table 1). Vertical columns of wooden beads (4 mm diameter) were inserted in the till to assess the strain distribution near the hemispheres. In most experiments, at least three bead columns were placed across the path of each hemisphere (30, 58 and 85 mm from the inner wall), and two columns were placed at far-field locations.

Experiments were conducted to displacements sufficiently large to allow steady-state drag forces and pore pressures to be approached. The hemispheres were pushed at speeds ranging from 15 to 400 m a−1, similar to the sliding speeds of many glaciers (Reference PatersonPaterson, 1994, p.134). Each test was conducted under a total normal stress of 65 kPa, equal to that during consolidation and the same order as effective normal stresses measured beneath soft-bedded glaciers (e.g. Reference Engelhardt and KambEngelhardt and Kamb, 1997). In most experiments a quasi-steady state was reached, in which rates of change in drag forces and pore pressures were small (roughly ≤3% per 10 mm displacement). Then ploughing was stopped, and the non-hydrostatic pore-water pressures developed during ploughing were allowed to dissipate. The normal stress was then removed from the till specimen, the device was disassembled and the distribution of strain around each hemisphere was determined by measuring the locations of the marker beads. In most cases, moisture content and porosity were measured prior to consolidation and after experiments were completed (Table 1).

4. Results

During most tests shear stresses on the hemispheres (bed-parallel drag force/plan-view area of hemisphere) increased rapidly upon initial displacement. Shear stresses then either peaked with a subsequent decline to a quasi-steady value (Fig. 4a) or, more commonly, they increased at a decreasing rate, asymptotically approaching a steady value (Fig. 4b and c). Pore pressures usually reached steady or quasi-steady values with sufficient displacement (Fig. 4a and b). An exception occurred in experiments at high ploughing speeds with the Engabreen till, in which excess pore pressures were decaying toward hydrostatic values when experiments were terminated (Fig. 4c); at lower ploughing speeds with this till, pore pressures became nearly hydrostatic with sufficient displacement (Fig. 4b). Behind hemispheres, steady pore-water pressures were usually slightly negative, reflecting suction (Fig. 4).

Fig. 4.

Results of ploughing experiments with (a) large hemisphere and Des Moines Lobe till (380 m a−1), (b) small hemisphere and Engabreen till (50 m a−1) and (c) large hemisphere with Engabreen till (50 m a−1). Dashed horizontal line indicates hydrostatic pore pressure (∼0.5 kPa).

Magnitudes of steady-state pore-water pressures varied with ploughing speed and with till hydraulic diffusivity (Fig. 5). In experiments with the Des Moines Lobe till, the magnitude of excess pore-water pressures in front of each hemisphere ranged from 30 to 122 kPa and, in general, increased with increasing ploughing speed (Fig. 5a). Data from the large hemisphere during one experiment (100 m a−1) were excluded because steady shear stresses were not approached during the test. Excess pore-water pressures observed in experiments with the more diffusive Engabreen till were significantly smaller, varying from 1 to 18 kPa (Fig. 5b). Pore-water pressures in front of the large hemisphere tended to be slightly larger than those in front of the small hemisphere.

Fig. 5.

Steady pore-water pressure in front of hemispheres (sensor 3, Fig. 3) as a function of ploughing velocity for experiments with (a) the Des Moines Lobe till and (b) the Engabreen till. Each pair of data points at a particular speed represents results of one experiment, with open circle the small hemisphere and filled circle the large hemisphere. Arrows in (b) indicate that pore pressure was decreasing when the experiment was terminated.

The effect of ploughing speed on steady-state shear stresses depended on till diffusivity (Fig. 6). Shear stresses in experiments with Des Moines Lobe till decreased exponentially with ploughing speed (R 2 = 0.85), and by a factor of 3.0–6.6 over the full range of speed (Fig. 6a). In experiments with the Engabreen till, shear stresses on the hemispheres increased slightly with ploughing speed. However, linear regression of the Engabreen data yields a low coefficient of determination (R 2 = 0.32) (Fig. 6b) and has power 0.49, well below that necessary to correctly describe the dependence on ploughing speed with greater than 95% confidence (0.8 (Reference CohenCohen, 1988)). In contrast, the power of the regression of shear stress on ploughing speed for experiments with the Des Moines Lobe till (0.995) greatly exceeds that threshold.

Fig. 6.

Steady shear stress on hemispheres, normalized to the mean steady-state shear stress, for experiments with (a) the Des Moines Lobe till and (b) the Engabreen till. Each pair of data points at a particular speed represents results of one experiment.

The normal stress on the sensing face (18 mm in diameter) in the upper platen was also measured in three additional experiments using the large hemisphere and the Des Moines Lobe till (Fig. 7). This measurement was made as the hemisphere passed beneath the sensing face to assess the impact of the upper platen on the stress state and resultant strength of the till in front of the hemisphere. During these experiments, conducted at speeds of 15, 30 and 380 m a−1, the stress began to increase sharply when the leading edge of the hemisphere was, respectively, ∼120, 150 and 350 mm from the load cell. In each case, peak normal stresses occurred ∼50 mm in front of the midpoint of the hemisphere (Fig. 7), comparable to the hemisphere diameter (40 mm). Peak stresses were 250, 165 and 110 kPa, respectively. Similarly to steady shear stresses on hemispheres in experiments with the Des Moines Lobe till, the magnitudes of the measured peaks in local normal stress were inversely correlated with ploughing speed.

Fig. 7.

Local normal stress (sensing face 18 mm in diameter) on the upper platen near the large hemisphere in experiments at three different ploughing speeds with the Des Moines Lobe till. Plots have been smoothed with a 4–5 mm running mean. Horizontal dashed line is the normal stress, averaged over the area of the upper platen. Lines with arrows at each end show the distance between where the peak local normal stress was measured and the top of the hemisphere.

Bead-displacement profiles (Fig. 8) indicated the formation of a till wedge in front of each hemisphere, which was immobile relative to adjacent till. This wedge was vertically and longitudinally more extensive in the Engabreen till. Upon excavation of the specimens after tests, a cavity with transverse dimensions nearly equal to those of the hemisphere was usually observed behind each hemisphere (Fig. 9a). This cavity was usually filled with soft, seemingly liquefied till. Cavities were elongate, forming a groove in overlying till that extended behind each hemisphere along the length of its path (Fig. 9b).

Fig. 8.

Bead locations at the conclusions of experiments with the large hemisphere: (a) Des Moines Lobe till and (b) Engabreen till. Plots are at the same scales. Dashed line indicates top of till specimen. Arrows indicate locations of initially vertical bead profiles. Light gray beads in (a) were displaced prior to ploughing due to strain during consolidation.

Fig. 9.

(a) Cavity in Engabreen till behind the large hemisphere at the conclusion of an experiment. (b) Groove in the base of an inverted section of a specimen of Des Moines Lobe till, formed behind the small hemisphere (visible near bottom with seemingly liquefied till behind it).

5. Modeling Measured Shear Stresses

An important question, owing in part to the likely effect of the sample-chamber boundaries on shear stresses, is whether measured shear stresses on the hemispheres can be reconciled with data and theory developed for the study of cone penetration through sediments. Theoretical models of cone penetration, in conjunction with cone-penetration data, are used routinely to estimate Coulomb frictional properties of sediments. The theory of Reference Senneset, Janbu, Chaney and DemarsSenneset and Janbu (1985) is most appropriate for our purposes because ploughing resistance is expressed in terms of effective stress. Also, the theory accounts for excess pore-water pressures that may be generated in sediments of low diffusivity, and it is reasonably applicable to different geometries, including a hemisphere.

For a hemisphere ploughing through water-saturated till, this theory indicates that the force on the leading edge of the hemisphere, F s, can be expressed as

(1)

where A c is the cross-sectional area of the hemisphere normal to the ploughing direction, p is the total normal stress, p′ is the ambient effective normal stress in the till bed (equal to p − u 0, where u 0 is ambient pore-water pressure), u f is excess pore-water pressure in front of the hemisphere, c is cohesion, and N q and N u are dimensionless bearing capacity factors dependent upon the friction angle, φ, of the till. If u f = 0, then Equation (1) corresponds to fully drained conditions. The bearing capacity factors are defined as

(2)

(3)

Measurements from experiments with cones, piles and plates agree reasonably well with Equations (2) and (3) (Reference Senneset, Janbu, Chaney and DemarsSenneset and Janbu, 1985). Given that for a hemisphere of radius r, A c = πr 2/2 and the shear stress parallel to the ploughing direction is τ s = F s/πr 2, the shear stress on a hemisphere is

(4)

In addition to the drag associated with the shear strength of till, another component of drag arises due to the pore-pressure gradient around the hemisphere associated with pore-water flow in the direction opposite that of ploughing. This seepage-force effect is not included in the analysis of Reference Senneset, Janbu, Chaney and DemarsSenneset and Janbu (1985). In our experiments, excess pore-water pressure was measured in front of and behind the hemispheres (u f and u b, respectively), so the component of water pressure parallel to the ploughing direction at any point along the surface of a hemisphere can be estimated as (u f − kθ) cos θ, where k = (u f − u b)/π (Fig. 10). The local surface over which this water pressure acts is r 2 sin θ dθ dα. Thus, the local shear force is equal to (u f − kθ) cos θ r 2 sin θ dθ dα. When this force is integrated over the surface of the hemisphere, the total shear force, F w, due to the excess pore-pressure gradient is expressed as

(5)

Integrating Equation (5) twice and dividing the result by the area of the hemisphere, πr 2, yields the shear stress due to seepage drag, τ w:

(6)

The total ploughing resistance, τ, is the sum of the resistance due to the till shear strength (Equation (4)) and the seepage drag of water around the hemisphere:

(7)

Application of this model to our results requires acknowledging that the boundaries of the sample chamber probably constricted till deformation past the hemispheres, thereby causing shear stresses on the hemispheres that were larger than in the absence of such boundaries. To approximately account for this effect, we used our measurements of local normal stress on the upper platen during the three experiments with the Des Moines Lobe till for which such data were available (Fig. 7). This stress, which was increased by the passage of the hemisphere due to the limited space for till deformation between it and the upper platen and walls, provides an estimate of total normal stress, p, as used in Equation (1). Thus we can compare calculated and measured shear stresses for these three experiments in which local normal stresses were measured. Total normal stresses used in the calculation were spatially averaged values determined by integrating the measured local stresses over the entire zone of influence as the hemisphere passed under the load cell (Fig. 7). The integrated values were 142, 96 and 68 kPa, for the three ploughing velocities (15, 30 and 380 m a−1, respectively).

Fig. 10.

Variables used for determining the seepage-related component of shear stress. The variables u f and u b are excess pore-water pressure at the locations indicated.

Other parameter values for the calculation are presented in Table 2. Pore-pressure data used in the calculation were the steady values measured nearest to the hemisphere (at pressure sensors 1 and 2 in Fig. 3). Hydrostatic water pressure (0.5 kPa) was used to calculate the ambient effective normal stress, p′, required in Equation (4).

Table 2.

Parameters used in model calculation

Shear stresses calculated from Equation (7) fall within 3%, 38% and 27% of measured values for the experiments at 15, 30 and 380 m a−1, respectively (Fig. 11). We view this agreement as quite good, given that there were no adjustable parameters and the approximate way that the sample-chamber boundaries were factored into the calculation. The calculated fraction of the total shear stress due to seepage drag (Equation (6)) was no more than 0.34 kPa, so seepage drag was subordinate to the drag associated with the till strength. This observation accounts for the inverse relationship between the magnitude of excess pore pressures and ploughing resistance (Figs 5a and 6a).

Fig. 11.

Shear stresses on the large hemisphere in experiments with the Des Moines Lobe till compared with shear stresses calculated using cone-penetration theory and measured values of pore-water pressure, local normal stress (Fig. 7) and the friction angle of the till.

6. Discussion

6.1. Laboratory results

These results demonstrate the pore-pressure feedback that can potentially cause velocity weakening at the surface of a soft bed and the dependence of this feedback on till properties. In experiments with the Des Moines Lobe till, there was a reduction in steady-state ploughing resistance by a factor of 3.0–6.6 over ploughing speeds ranging from 15 to 380 m a−1 (Fig. 6a), and most of this reduction occurred over about a six-fold increase in velocity from 15 to 90 m a−1. This weakening was caused by increases in excess pore pressure, driven by compaction of till in front of the hemispheres, which reduced the till shear strength (Fig. 5a).

Owing to the much higher hydraulic diffusivity of the Engabreen till, results of experiments with it were quite different. Excess pore-water pressures in front of the hemispheres were, at most, only ∼20% of those observed in the Des Moines Lobe till, and positive pore pressures were still decreasing when experiments at high speeds were terminated. Consequently, there was no convincing evidence of velocity weakening.

The shear stresses on the small hemisphere were generally larger than those measured on the large hemisphere: as much as 2.5 times larger with the Engabreen till (Fig. 4) and as much as 65% larger in the lowest-velocity experiments with the Des Moines Lobe till (Fig. 12). These differences are too large to attribute to pore-pressure effects alone. We speculate that these differences may be related to unmeasured local stress differences associated with the boundary effects of the sample chamber, but we lack sufficient data to provide a definitive explanation. Results for a given till and hemisphere illustrate velocity-dependent trends of shear stress and pore pressure that are generally consistent.

Fig. 12.

(a) Shear stress on the hemispheres as a function of ploughing speed in our experiments with the Des Moines Lobe till. (b) Stress on the face of a cone, 11.3 mm in diameter, required to push it through two mixtures of clay and sand at various speeds in calibration-chamber experiments (from Reference KimKim, 2005).

Deformation kinematics were also different for the two tills (Fig. 8). Strain was focused nearer the hemispheres in experiments with the Des Moines Lobe till. The Des Moines Lobe till has a lower friction angle (18.5° (Reference Hooyer and IversonHooyer and Iverson, 2002)) and contains more clay than the sand-rich Engabreen till (32.0° (Reference MooreMoore, 2002)). This result is consistent with previous experiments with the ring-shear device in which strain in the specimen chamber was more localized in a clay-rich till than in a clay-poor till, reflecting, perhaps, either the tendency for clay minerals to align during shear and limit expansion of a shear zone (Reference Iverson, Baker and HooyerIverson and others, 1997) or the tendency for shear-zone thicknesses in granular media to depend on grain diameter (Reference Tulaczyk, Mickelson and AttigTulaczyk, 1999).

6.2. Related laboratory data

Geotechnical cone-penetration experiments in laboratory ‘calibration chambers’ demonstrate that excess pore pressures and speed-dependent reductions in ploughing resistance observed in our experiments with Des Moines Lobe till are in no way unique to the particular configuration of our experiment. In these experiments a rod with a cone-shaped end is pushed parallel to the rod axis at a constant speed through sediment contained in a chamber many times larger in diameter than the rod. The most illuminating experiments, to date, were conducted by Reference KimKim (2005). He used a calibration chamber with a diameter 106 times larger than the rod and measured both pore pressure immediately adjacent to the cone and the stress on the cone face (bearing resistance) required to push it at a constant speed through mixtures of clay and sand.

Results indicated a dependence of excess pore pressure and stress on the cone as a function of ploughing speed quite similar to that of this study (Fig. 12). Other experiments by Reference KimKim (2005) with slightly different mixtures of clay and sand and different shapes of ploughing elements yielded similar results. Moreover, the same inverse relationship between ploughing speed and resistance has been observed in many other geotechnical studies (e.g. Reference Finnie, Randolph and ChryssostomidisFinnie and Randolph, 1994; Reference Finke, Mayne and KloppFinke and others, 2001; Reference House, Oliveira and RandolphHouse and others, 2001). Therefore, the excess pore pressures and velocity weakening we observed are unlikely to be artifacts of the particular design of our experiments.

The only laboratory ploughing experiments conducted with till, apart from those of this study, were those of Reference RousselotRousselot (2006) (see also Reference Rousselot and FischerRousselot and Fischer, 2007), who used a customized apparatus to push a vertical rod horizontally through water-saturated till in a large chamber. These experiments approximated the action of a plough-meter, an instrumented rod that can be driven into a soft bed through a borehole and used to study soft-bed mechanical properties (Reference Fischer and ClarkeFischer and Clarke, 1994). The force on the rod was measured at different ploughing speeds, and pore pressure was recorded at many locations around the perimeter of the rod. Although excess pore pressures in front of the rod increased with the rod speed, values did not exceed ∼15 kPa and hence were as low as those measured with the Engabreen till (Fig. 5b). Ploughing velocities (365–6200 m a−1) were about an order of magnitude higher than in this study, but particularly significant was the hydraulic diffusivity of the sediment used: 5 × 10−5 m2 s−1. This value is approximately a factor of 140 and 5700 greater than that of the Engabreen and Des Moines Lobe tills, respectively (Table 1). No velocity weakening was observed. In the following section we show that the high diffusivity of the sediment used by Reference RousselotRousselot (2006) accounts for the low excess pore pressure measured in that study and the lack of velocity weakening.

6.3. Conditions for pore-pressure feedback and velocity weakening

The conditions under which excess pore pressure and velocity weakening are expected can be estimated by comparing characteristic timescales of compaction and pore-pressure diffusion in till down-glacier from a ploughing particle. If the latter exceeds the former, then pore-pressure diffusion cannot keep pace with pore-pressure generation in the compacted zone, resulting in significant excess pore pressure and velocity weakening. The timescale for compaction, t C, is b/V p, where b is the characteristic length scale over which the till compacts and V p is ploughing speed (Reference IversonIverson, 1999). The value of b was within ±20% of the hemisphere diameters, as indicated by bead displacements in our experiments (e.g. Fig. 8). Geotechnical studies (Reference Malyshev, Lavisin and BromsMalyshev and Lavisin, 1974; Reference Koumoto, Kaku, Verruijt, Beringen and de LeeuwKoumoto and Kaku, 1982) also indicate that the zone of sediment compaction in front of a ploughing object is roughly comparable to its diameter, so we consider δ to equal the hemisphere diameters. The characteristic timescale for pore-pressure diffusion, t D, is δ2/D, where D is the hydraulic diffusivity of the till (Reference IversonIverson, 1999) and δ equals the length of the diffusion path. Thus,

(8)

If t D/t C > 1.0, significant excess pore pressure and velocity weakening are expected.

Figure 13 shows excess pore pressures measured in the two tills of this study and those measured in the glacial sediment used by Reference RousselotRousselot (2006), plotted as a function of t D/t C. Excess pore pressures are clearly correlated to conditions for which this ratio exceeds 1.0. This ratio was generally greater and less than 1.0, respectively, for experiments with the Des Moines Lobe and Engabreen tills, owing to the 40-fold difference in their diffusivities. Thus, only the Des Moines Lobe till exhibited clear velocity weakening (Fig. 6a). Although ploughing velocities in the study of Reference RousselotRousselot (2006) (see also Reference Rousselot and FischerRousselot and Fischer, 2007) were about an order of magnitude higher than in this study, the much higher diffusivity of the sediment in that study (more than two orders of magnitude) results in t D/t C<1.0, which accounts for the low excess pore pressures (Fig. 13) and lack of velocity weakening observed in that study.

Fig. 13.

Excess pore pressure as a function of t D/t C, the ratio of the characteristic timescales of pore-pressure diffusion and compaction, from the ploughing experiments of this study and from those of Reference RousselotRousselot (2006). Measurements from the latter study are from a sensor about one rod-diameter in front of the ploughing rod.

Having established that timescales for compaction and pore-pressure diffusion provide an effective means of estimating the conditions under which velocity weakening is expected, we can use these timescales to explore glacially relevant ranges of parameter space over which velocity weakening will occur. Setting the two timescales equal allows a transitional ploughing velocity, V t = D/δ, to be defined, above which there will be significant velocity weakening. We again consider δ to be equal to the particle diameter and additionally acknowledge that ploughing speeds will be less than, but commonly comparable to, the slip velocity of ice over the till surface (Reference Iverson and HooyerIverson and Hooyer, 2004; Reference IversonIverson and others, 2007), particularly when till is weak and ploughing resistance is low. If we, therefore, equate ploughing velocity with slip velocity, ranges of till hydraulic diffusivity (Reference Freeze and CherryFreeze and Cherry, 1979, p.29, 55) and sizes of ploughing particles can be defined over which velocity weakening will occur for a particular slip velocity.

Figure 14 indicates that excess pore pressures and velocity weakening are expected over a wide range of slip velocity, till diffusivity and ploughing-particle size. Thus, activation of this velocity-weakening mechanism might occur over an increasing fraction of a soft bed as a glacier increases its sliding speed due to, for example, changing basal hydrology.

Fig. 14.

Ranges of till diffusivity and sizes of ploughing particles over which significant excess pore pressure and velocity weakening will occur for different transitional glacier slip velocities, V t, for which t D/t C = 1.

6.4. Experimental deviations from the subglacial system

The most obvious difference between these experiments and ploughing in a subglacial setting is the lack of ice flow past ploughing particles. This flow, by regelation and creep past particles at a speed proportional to the ploughing resistance, will result in a zone of reduced total normal stress down-glacier from particles. The resultant reduction in effective stress on the bed there reduces the local till strength and ploughing resistance (Reference Brown, Hallet and BoothBrown and others, 1987; Reference IversonIverson, 1999). The effect is small, however, because for most particle sizes at the ice–bed interface, bed-parallel re-gelation will be the dominant ice-flow mechanism (e.g. Reference IversonIverson, 1999). The theory of Reference NyeNye (1967) then predicts a reduction of total normal stress on the bed down-glacier from ploughing particles of only ∼10% (Reference Brown, Hallet and BoothBrown and others, 1987). Also, if regelation infiltration of the bed occurs (Reference ClarkeClarke, 2005), as has been observed subglacially with resultant ice-cemented till overlying a soft bed (Reference IversonIverson and others, 2007), bed-parallel ice flow past ploughing particles will be inhibited by frictional interaction among grains in the ice-cemented layer.

Pore-water drainage in our experiments must also be considered. In the ring-shear device, the permeable upper platen of the sample chamber (Fig. 3) is the single boundary where drainage of pore-water could occur. Its close proximity to the hemispheres (≤50 mm) is likely to have limited the timescale for diffusion and the magnitude of excess pore pressures.

Finally, the close proximity of the upper platen and walls of the specimen chamber to the hemispheres caused the strength of till near each hemisphere to be larger than would be the case subglacially. In applying cone-penetration theory (section 5), the effect of the upper platen was accounted for approximately by measuring the local total normal stress near the hemispheres (Fig. 7). Considerable supporting geotechnical data (section 6.2) indicate that this boundary effect did not obscure the relationships between ploughing speed, excess pore pressure and ploughing resistance that these experiments were designed to explore.

7. Implications

7.1. Ploughing models

No model of subglacial ploughing accounts for the pore-pressure feedback and velocity weakening observed in these experiments. Models that consider till a viscous or visco-plastic fluid (Reference AlleyAlley, 1989) predict velocity strengthening during ploughing and are not supported by our results. Other models make the more experimentally tenable assumption that till behaves as a Coulomb-plastic material but neglect the pore-pressure feedback. The models of Reference Brown, Hallet and BoothBrown and others (1987), Reference IversonIverson (1999) and Reference IversonIverson and others (2007) are strictly applicable to only the so-called drained case, in which till is sufficiently diffusive or sliding velocity is sufficiently small that significant excess pore pressures do not develop. The ploughing model of Reference Tulaczyk, Mickelson and AttigTulaczyk (1999), in contrast, is strictly applicable to only the undrained case, in which till diffusivity is sufficiently small relative to sliding speed that there is effectively no pore-pressure dissipation. Tulaczyk calculated that ploughing resistance should differ between these two cases by a factor of 2.1–3.9. Our results (Fig. 6) and those of Reference KimKim (2005) (Fig. 12b) demonstrate reductions in ploughing resistance moving from largely drained to undrained conditions that are comparable.

Our new ploughing model (section 5) includes excess pore pressures and their effects on both till strength and seepage drag. Predictions of ploughing resistance with no adjustable parameters were within, in the worst case, 38% of measured values over a wide range of ploughing speeds and excess pore pressures. The primary limitation of the model is that pore pressure needs to be measured independently. Computing steady pore-pressure distributions near particles using ploughing speed, sizes of ploughing particles and till hydrological properties would be an important next step in modeling ploughing.

7.2. Glacier flow and sediment transport

Basal motion tends to be focused near the surface of soft beds when basal-water pressure is high (Reference Blake, Fischer and ClarkeBlake and others, 1994; Reference Iverson, Hanson, Hooke and JanssonIverson and others, 1995, Reference Iverson2003, Reference Iverson2007; Reference Engelhardt and KambEngelhardt and Kamb, 1997; Reference Truffer and HarrisonTruffer and Harrison, 2006), indicating that, when the bed is especially weak, ploughing, rather than the classical sliding mechanisms, is the likely slip mechanism. Our results indicate that in this case, contrary to what is usually assumed in models of soft-bedded glaciers, resistance to basal slip can be less than the ambient Coulomb yield strength of the till, owing to pore-pressure feedback that effectively weakens till near the glacier sole.

However, for this process to be a potentially important velocity-weakening mechanism a significant fraction of the bed that is in contact with ice must consist of particles sufficiently large to undergo rate-dependent ploughing. Particularly for fine-grained tills, the water layer at the bed surface (e.g. Reference Brown, Hallet and BoothBrown and others, 1987; Reference AlleyAlley, 1989; Reference Tulaczyk, Mickelson and AttigTulaczyk, 1999) will tend to submerge a fraction of the bed area, over which there will be effectively no resistance to basal motion. Thus, a key question is whether rate-dependent ploughing is likely over a significant fraction of the remaining unsubmerged area of the bed. To explore this issue for the fine-grained Des Moines Lobe till we note that, like some other basal tills, there is a power-law relationship between the number of grains of a given size class and grain size (Reference Hooke and IversonHooke and Iverson, 1995). This relationship allows the proportion of the unsubmerged fraction of the bed occupied by particles above a threshold size to be calculated as a function of water-layer thickness and of only two parameters that describe the grain-size distribution: the power-law exponent (fractal dimension) and maximum grain size of the till (Reference IversonIverson, 1999). In Figure 15 we consider two size thresholds, 2 and 10 mm, above which rate-dependent ploughing will be expected for reasonable ranges of sliding speed and till diffusivity (Fig. 14). The fractal dimension of the Des Moines Lobe till is 2.96 (Reference Hooyer and IversonHooyer and Iverson, 2002) and because the maximum grain size is difficult to measure or estimate we consider two quite different values, 0.1 and 1.0 m. Even for water-layer thicknesses as small as 1 μm, 25–55% of the bed area in contact with ice will be subject to velocity weakening (Fig. 15). Choosing a water-layer thickness of 0.1 mm, equal to that inferred for Whillans Ice Stream (Reference Engelhardt and KambEngelhardt and Kamb, 1997), yields 40–77% of the bed area. Thus, it would appear that the bed area affected by this velocity-weakening mechanism can be significant. A potential effect of this weakening during glacier speed-up would be to progressively shift the downslope component of the glacier weight elsewhere, causing longitudinal and lateral stress gradients and ultimately further increasing the speed of the glacier.

Fig. 15.

Fractional area of the bed that is not submerged by the water layer occupied by grains larger than 2 and 10 mm in diameter, as a function of water-layer thickness, for the grain-size distribution of the Des Moines Lobe till. Grains 2 and 10 mm in diameter are sizes above which ploughing-induced velocity weakening is likely for common ranges of sliding speed and till diffusivity. The fractal dimension of the grain-size distribution is 2.96 (Reference Hooyer and IversonHooyer and Iverson, 2002), and two different maximum grain sizes (d max) for the size distribution are assumed for each of the two size thresholds. The till porosity is assumed to be 0.35.

Pervasive bed deformation has been commonly invoked as a mechanism for high glacial sediment fluxes (e.g. Reference AlleyAlley, 1991, Reference Alley, Maltman, Hubbard and Hambrey2000; Reference Jenson, Clark, MacAyeal, Ho and VelaJenson and others, 1995; Reference BoultonBoulton, 1996; Reference Dowdeswell and SiegertDowdeswell and Siegert, 1999; Reference Siegert and DowdeswellSiegert and Dowdeswell, 2002). Our finding that ploughing resistance can decrease with increasing ploughing speed has clear implications for the bed-normal distribution of velocity in a soft bed: high rates of basal motion might create a weak till layer near the glacier sole where shear strain would be focused due to ploughing. Thus, a smaller thickness of the bed would be subjected to shear, with a potentially reduced sediment flux.

7.3. Basal seismicity

Velocity weakening plays a central role in explanations of rapid slip on crustal faults (e.g. Reference ScholzScholz, 2002, p.82). If slip resistance on a fault decreases with slip velocity, then a force imbalance can develop that briefly causes acceleration of fault-bounding rocks sufficient to generate seismic waves. A force imbalance results because, if rocks loading a fault are sufficiently compliant elastically, slip resistance can decrease faster than the rate at which the driving stress decreases on the fault due to elastic relaxation of adjacent rocks. Thus, there is a mismatch between the rate at which slip resistance declines and the rate at which stress transfer to other parts of the fault occurs. This mismatch results in rock acceleration, followed by deceleration once driving and resisting stresses have become equal after sufficient relaxation of fault-bounding rocks (see fig. 2.16 in Reference ScholzScholz, 2002).

Although processes responsible for glacier seismicity are difficult to isolate definitively (e.g. Reference Deichmann, Ansorge, Scherbaum, Aschwanden, Bernardi and GudmundssonDeichmann and others, 2000; Reference Ekström, Nettles and TsaiEkström and others, 2006; Reference Tsai and EkströmTsai and Ekström, 2007), at least some seismicity is clearly caused by basal-slip processes (Reference Anandakrishnan and BentleyAnandakrishnan and Bentley, 1993; Reference Anandakrishnan and AlleyAnandakrishnan and Alley, 1994, Reference Anandakrishnan and Alley1997). As part of a soft-bedded glacier speeds up, for whatever reason, it may exceed the transitional slip velocity (Fig. 14) required for widespread velocity weakening. Glaciers can behave elastically over periods of minutes to 1 day (Reference Bahr and RundleBahr and Rundle, 1996) and are elastically more compliant than crustal rocks. This compliance increases the likelihood of a brief force imbalance at the bed. Moreover, the extent of velocity weakening observed in this study is orders of magnitude greater than the fault-gouge velocity weakening sufficient to generate crustal earthquakes (Reference ScholzScholz, 2002, p.85). In addition, in contrast to the velocity-weakening mechanism for a rigid bed (Reference SchoofSchoof, 2004), weakening occurs immediately with an increase in slip velocity, so that it can conceivably occur at a rate that is higher than the rate at which stress can be transferred to other parts of the bed through elastic relaxation of ice. Thus, we view the velocity-weakening mechanism of this study as a viable candidate for enabling basal seismicity.

8. Conclusions

When particles that couple a glacier to a till bed plough, slip resistance can depend inversely on ploughing velocity. As ploughing velocity increases, progressively higher excess pore pressures are generated down-glacier from ploughing particles, weakening till there and decreasing ploughing resistance. In our experiments, steady-state ploughing resistance decreased by a factor of 3.0–6.6 with a six-fold increase in sliding speed (e.g. Fig. 6). Timescales of till compaction and pore-pressure diffusion depend on ploughing velocity, sizes of ploughing particles and till hydraulic diffusivity, and accurately predict the ranges of these variables under which velocity weakening occurs. These ranges are within those relevant to many soft-bedded, wet-based glaciers, although basal tills of sufficiently high hydraulic permeability, and hence diffusivity, will not be subject to this effect. Small excess pore pressures without velocity weakening in laboratory ploughmeter experiments (Reference Rousselot and FischerRousselot and Fischer, 2007) resulted from the high diffusivity of the sediments used.

Existing models of ploughing fail to account for the observed pore-pressure feedback and velocity weakening, although those that assume Coulomb till behavior under either fully drained or undrained conditions can be adequate for specific ranges of ploughing-particle size, ploughing velocity and till diffusivity. The new ploughing model presented here accounts for the effect of excess pore pressure on till strength and seepage drag and provides an estimate of ploughing resistance within 3–38% of measured values. Velocity weakening at the surface of a soft bed by ploughing may help trigger fast glacier flow and inhibit deformation of the bed at depth. Velocity weakening is also a requirement for slip-induced basal seismicity.

Acknowledgements

We are grateful to B. Hubbard, S. Tulaczyk and an anonymous reviewer for comments that improved the paper. We also acknowledge J. Marchetti, formerly of the Electrical Engineering Machine Shop of the University of Minnesota, for his skilful fabrication of the ploughing insert for the ring-shear device. We also thank D. Nelsen for helping with preliminary experiments. This work was supported by the US National Science Foundation: OPP-9725360. Publication was authorized by the Chief, Illinois State Geological Survey.

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Figure 0

Fig. 1.(a) Ploughing particles at the ice–till interface. (b) Cobble-sized clast (ruler is 0.3 m long) that has ploughed from left to right through Illinoian glacial sediments in central Illinois, leaving a groove up-glacier and a prow down-glacier (Iverson and Hooyer, 2004). (c) More evidence of ploughing (from upper right to lower left) at the same location.

Figure 1

Fig. 2.(a) Cross-section of the ring-shear device, as adapted for ploughing experiments. Dark gray components rotate. (b) Detail of the specimen chamber with insert that contains the hemispheres. (c) Specimen chamber with only the large hemisphere visible at left.

Figure 2

Fig. 3.Longitudinal cross-section of the specimen chamber in the vicinity of the large hemisphere. Movement direction of the hemisphere and adjacent insert is from left to right. The upper platen is fixed rotationally but can move up and down.

Figure 3

Table 1.Till properties and experimental conditions

Figure 4

Fig. 4.Results of ploughing experiments with (a) large hemisphere and Des Moines Lobe till (380 m a−1), (b) small hemisphere and Engabreen till (50 m a−1) and (c) large hemisphere with Engabreen till (50 m a−1). Dashed horizontal line indicates hydrostatic pore pressure (∼0.5 kPa).

Figure 5

Fig. 5.Steady pore-water pressure in front of hemispheres (sensor 3, Fig. 3) as a function of ploughing velocity for experiments with (a) the Des Moines Lobe till and (b) the Engabreen till. Each pair of data points at a particular speed represents results of one experiment, with open circle the small hemisphere and filled circle the large hemisphere. Arrows in (b) indicate that pore pressure was decreasing when the experiment was terminated.

Figure 6

Fig. 6.Steady shear stress on hemispheres, normalized to the mean steady-state shear stress, for experiments with (a) the Des Moines Lobe till and (b) the Engabreen till. Each pair of data points at a particular speed represents results of one experiment.

Figure 7

Fig. 7.Local normal stress (sensing face 18 mm in diameter) on the upper platen near the large hemisphere in experiments at three different ploughing speeds with the Des Moines Lobe till. Plots have been smoothed with a 4–5 mm running mean. Horizontal dashed line is the normal stress, averaged over the area of the upper platen. Lines with arrows at each end show the distance between where the peak local normal stress was measured and the top of the hemisphere.

Figure 8

Fig. 8.Bead locations at the conclusions of experiments with the large hemisphere: (a) Des Moines Lobe till and (b) Engabreen till. Plots are at the same scales. Dashed line indicates top of till specimen. Arrows indicate locations of initially vertical bead profiles. Light gray beads in (a) were displaced prior to ploughing due to strain during consolidation.

Figure 9

Fig. 9.(a) Cavity in Engabreen till behind the large hemisphere at the conclusion of an experiment. (b) Groove in the base of an inverted section of a specimen of Des Moines Lobe till, formed behind the small hemisphere (visible near bottom with seemingly liquefied till behind it).

Figure 10

Fig. 10.Variables used for determining the seepage-related component of shear stress. The variables uf and ub are excess pore-water pressure at the locations indicated.

Figure 11

Table 2.Parameters used in model calculation

Figure 12

Fig. 11.Shear stresses on the large hemisphere in experiments with the Des Moines Lobe till compared with shear stresses calculated using cone-penetration theory and measured values of pore-water pressure, local normal stress (Fig. 7) and the friction angle of the till.

Figure 13

Fig. 12.(a) Shear stress on the hemispheres as a function of ploughing speed in our experiments with the Des Moines Lobe till. (b) Stress on the face of a cone, 11.3 mm in diameter, required to push it through two mixtures of clay and sand at various speeds in calibration-chamber experiments (from Kim, 2005).

Figure 14

Fig. 13.Excess pore pressure as a function of tD/tC, the ratio of the characteristic timescales of pore-pressure diffusion and compaction, from the ploughing experiments of this study and from those of Rousselot (2006). Measurements from the latter study are from a sensor about one rod-diameter in front of the ploughing rod.

Figure 15

Fig. 14.Ranges of till diffusivity and sizes of ploughing particles over which significant excess pore pressure and velocity weakening will occur for different transitional glacier slip velocities, Vt, for which tD/tC = 1.

Figure 16

Fig. 15.Fractional area of the bed that is not submerged by the water layer occupied by grains larger than 2 and 10 mm in diameter, as a function of water-layer thickness, for the grain-size distribution of the Des Moines Lobe till. Grains 2 and 10 mm in diameter are sizes above which ploughing-induced velocity weakening is likely for common ranges of sliding speed and till diffusivity. The fractal dimension of the grain-size distribution is 2.96 (Hooyer and Iverson, 2002), and two different maximum grain sizes (dmax) for the size distribution are assumed for each of the two size thresholds. The till porosity is assumed to be 0.35.