Introduction

The use of radioisotopes for measurement of snow density is not new. Reference GerdelGerdel and others (1950) report on a radiotelemetering snow gage used successfully to measure up to 55 water-equivalent inches (1.4 m.) of a snow-pack using the principle of absorption by water of gamma emissions from a cobalt 60 source. Reference BaderBader and others (1951, p. 15–18 and 41) discuss an X-ray density scanning technique and instrument which determined the density of snow by measuring the attenuation of a transmitted beam of X-rays in accordance with Lambert’s law. In general these transmission techniques require a collimated source-detector combination, separated a known distance. For profiling snow densities this also requires simultaneous lowering of a source and detector in separate holes.

Geophysical exploration in the petroleum industry was responsible for the initial development of present-day radioactive well-logging techniques. Use of neutrons for drill-hole surveying was first suggested and tested by Reference PontecorvoPontecorvo (1941). His technique utilized a detector in close proximity to the source in a single probe and as such was the first use of the reflectance or scattering technique.

First use of nuclear probes to investigate soils for engineering purposes was reported by Reference BelcherBelcher and others (1950). Their equipment consisted of two probes. One probe, which measured the moisture or hydrogen content of the soil, had a neutron source with foil or Geiger tube detectors, and the other probe, which measured soil density, used a gamma-ray source and a Geiger tube detector.

Reference Leighty and FrankensteinLeighty and Frankenstein (unpublished) made limited tests on snow and ice with a surface soil-moisture gage and found the neutron count rate to be a linear function of density over the sampled density range of 0.31 to 0.92 g./cm.³. Reference GayGay (1962); Reference AndersonAnderson and others (1962, 1963) and Reference AndersonAnderson (1963) report on the use of a depth moisture probe and a depth density probe for investigating snow-pack profiles within the density range of 0.11 to 0.52 g./cm.³ in the Rocky Mountains.

Early in 1962 United States Army Cold Regions Research and Engineering Laboratory research funds to investigate nuclear techniques for measurements of snow density were made available. A rapid method of direct determination of snow density by logging the count rate of a neutron probe lowered in a hole at a continuous rate was envisioned. A commercial neutron probe satisfied the requirements for a fixed geometric relationship between source and counter to ensure reproducible measurements, since the method consists in measuring the density of scattered neutrons at a given distance from the source. Prior to the field work it was realized that such a commercially available soil-moisture depth probe might not have the desirable characteristics for optimum determination of snow density profiles, but experience gained from its use would point to later modifications to improve the technique if justified. This paper discusses the preliminary field investigations conducted in Greenland during the period 8–19 May 1963.

Equipment and Procedure

The basic project equipment for nuclear measurement consisted of the nuclear probe, a scaler, a rate-meter and a chart recorder. The standard SIPRE snow observation kit, SIPRE 3-in. (7.6 cm.) coring auger kit and the

in. (3.8 cm.) auger from the SIPRE ice thickness kit were used to obtain gravimetric snow density samples and provide holes into which the nuclear probe was lowered. The probe, Nuclear Chicago Model P-19, Subsurface Soil Moisture Probe, had a 4.5 millicurie radium–beryllium fast neutron source and one boron floride thermal neutron detector tube with a sensitive length of 5.5 in. (14 cm.). The probe had an external diameter of in. (3.8 cm.) with a 50 ft. (15 m.) connecting cable graduated in 2 in. (5.08 cm.) increments.

Two modes of obtaining the nuclear data were used. Mode 1, the probe–rate-meterchart-recorder combination, produced a continuous chart record of the variation of the nuclear count rate with depth: Mode 2, the probe–scaler combination, produced a visual indication of the nuclear counts for a selected time duration when the probe was at a stationary position in the hole; repeating this count procedure at different selected depths allowed construction of a curve similar to that obtained with the rate-meter.

The general procedure for data collection consisted of (1) coring a vertical hole with the

in. (3.8 cm.) auger, (2) obtaining the profile of nuclear count rate versus depth using both Modes 1 and 2, and (3) determining the density profile of the snow by standard gravimetric sampling procedures with the 500 cm.³ (30.5 in.³) sample tubes from the snow observation kit and/or sections of the 3 in. (7.6 cm.) vertical core obtained with the coring auger.

Results

Because the nuclear determination of snow density is an indirect method, an initial correlation with the field sample density is necessary. Figure 1 shows the results of the correlation between scaler count ratio and the snow sample density; count ratio (which varies from 0 to 1.0 for any neutron probe) is the ratio of scaler count rate in snow to scaler count rate in water. The data in Figure 1 represent snow sample densities from 0.32 to about 0.70 and lake-ice densities of 0.87 to 0.91 g./cm.³ The maximum range in density for any given count ratio was from 0.40 to 0.70, a difference of 0.30 g./cm.³ This variation is unacceptable for profiling snow stratigraphy; however, the major portion of the variation may be related to the inexperience of the snow samplers and to the difference between the effective sample volume in the nuclear method compared with that in the standard gravimetric method. Errors attributable to poor technique for obtaining and weighing samples and failure to sample a real density variation could contribute greatly to the discrepancies. The density at any given depth below the surface was seen to vary, and the density profile at the site of the nuclear measurements could have been different from that at the site of the standard density measurements. The largest source of error, however, is attributed to sample volumes. In snow of density 0.40 g./cm.³ it is estimated that the effective diameter of the neutron cloud around the source is 41.5 cm. (16.3 in.) a spherical volume of about 37,000 cm.³ (2,300 in ³). This is about 74 times as great as the 500 cm.³ (30.5 in.³) from the density sample tube and more than 100 times as great as a 3-in. (7.6 cm.) section of snow from the 3-in. (7.6 cm.) coring auger. A variation in density of snow within the neutron sphere will affect the count rate and may not be detected by the density sampling of a novice.

Fig. 1. Scaler count ratio plotted against sampled snow density in g./cm.³

Reference AndersonAnderson and others (1963) present a formula for a regression curve for count rate and snow density with the P-19 probe. The computed results, divided by their water count, are presented by the circled points in Figure 1. There is reasonable agreement between the project data and a line representing the mean of their correlation curve. It is thought that discrepancies should exist because of the difference in snow conditions of the Rocky Mountains and the Greenland Ice Sheet. The heavy snowfalls of the mountains, which usually measure feet (metres), tend to develop thick strata of uniform densities, while in Greenland snowfall is measured in inches (centimetres) and large density differences can be found in closely spaced strata of small thicknesses.

Field data obtained at the lower portion of the TUTO Ramp, on the ice sheet about one mile (1.6 km.) from the ice–land boundary, are shown in Figure 2. Here 4 ft. 4 in. (1.32 m.) of winter snow covered the glacial ice, so that an abrupt density difference existed at the snow–ice interface. As seen from this illustration, the sampled snow density ranged from 0.320 to 0.492 g./cm.³, while the sampled ice densities ranged from 0.863 to 0.901 g./cm.³. Not shown in this illustration were two thin ice lenses, each about

in. (0.8 mm.) in thickness, in. (79.5 cm.) and 40 in. (101.5 cm.) below the surface. Two-minute scaler counts, beginning 10 in. (25.4 cm.) below the surface and spaced every 6 in. (15.2 cm.) thereafter, are shown to approximate the variations in sample densities, except in the regions immediately below the snow–ice interface. The scaler measurement at 4 ft. 3 in. does not show the expected increase in count rate when the source was only one inch (2.54 cm.) above the ice and in. (3.8 cm.) of the detector tube was beneath the snow–ice interface. The diameters of the neutron cloud around the source in snow of 0.40 g./cm.³ density and ice of 0.90 g./cm.³ density are approximately 16 and 12 in. (41 and 30 cm.) respectively and since the scaler count rate at 5 ft. 3 in. seems to result entirely from the ice count, it is assumed that the snow–ice interface in the sample fit and in the probe hole were at different depths. This could be possible on the TUTO Ramp. A vertical difference of 6 in. in 20 ft. or so from probe hole is not an unreasonable variation for the ice surface, which is exposed to melt-water run-off each summer. The rate-meter curve obtained with a time constant of 2 sec. intersects most of the scaler points in Figure 2. Rate-meter curves at 10 sec. and 20 sec. time constants are smoother, follow only the general trend of the scaler points in the snow and ice, and show a gradual change in count rate for the probe travel up-hole through the snow–ice interface.

Fig. 2. Field data obtained on the lower portion of TUTO Ramp, Thule, Greenland, 16 May 1963, show the snow density profiles and nuclear profiles obtained by the scaler and rate-meter modes. The rate-meter curves were obtained during up-hole travel of the probe

With an assumed correlation curve of count rate versus snow density and curves for statistical deviations of neutron count rates, curves were constructed for statistical deviations in snow density at different probability levels for the scaler and rate-meter data. These curves, while not entirely correct, demonstrate that the nuclear technique has possibilities of producing the statistical accuracy for determining snow density profiles.

The reproducibility of the rate-meter curves was well within the theoretical statistical deviations at the 95 per cent probability level and this denotes that any deflection of the curves having duplication could be attributed to differences in snow density profile. As expected, when the

in. (3.8 cm.) probe was suspended in the center of a 5 in. (12.7 cm.) hole, the annulus of air surrounding the probe reduced the number of neutrons scattered back to the detector.

Summary

A direct record of snow density versus depth is a distinct possibility for the near future when the resolution of the profile stratigraphy can be improved by perfecting the source–detector combination. The rapidly advancing state of the art of nucleonics will provide increased resolution as well as increased accuracy.