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        Snow Wetness Measurement by Fluorescent Dye Dilution
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        Snow Wetness Measurement by Fluorescent Dye Dilution
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        Snow Wetness Measurement by Fluorescent Dye Dilution
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Abstract

The fluorescent dye dilution method for determining the liquid-water content in snow is based on measuring the concentration change of a solution when it is mixed with snow. Samples for analysis can be obtained rapidly and reliably, and, unlike calorimetric or equilibrium-temperature methods, field use requires no on-site data analysis.

Introduction

The change in concentration when an aqueous solution is mixed with wet snow provides a basis for measuring the liquid-phase fraction of snow. One method of measuring concentration changes uses a saline solution, which, when mixed in a dewar with a snow sample, produces a temperature depression in the mixture. The resulting solution concentration is determined from the equilibrium temperature, and the heat balance is calculated to adjust the result because of the liquid water produced by the brine and by the heat from the dewar. This method was proposed by Bader (1948, 1950) and recently improved by Morris (1981) who tested it in the field. Colbeck (1978) reviewed various techniques for measuring the liquid-water content of snow, and concluded that Bader’s method should be accurate, as long as the concentration of the original saline solution is accurately known.

Other techniques can be used to measure concentration changes directly, and considerable practical advantage is gained if solution samples can be extracted and stored for later analysis, eliminating the need for on-site data analysis. LaChapelle and Perla (unpublished) proposed the use of a spectrophotometer to determine the dilution of a dye solution.

In the method described in this paper, we use a fluorometer. A fluorescent dye solution at 0°C is added to a snow sample and a small amount is extracted after thorough mixing. If no phase change occurs, the change in concentration corresponds to the amount the dye was diluted by the liquid water in the snow sample. A favorable attribute of fluorescent dyes, in comparison to saline solutions, is that accurate measurement is possible with concentrations that produce negligible freezing-point depression.

Theory

A known mass of solution m1 at concentration C1 is added to a known mass of snow ms containing mass mi of ice and mass mw of liquid water. After mixing, the sample has liquid water content m1 +mw. The concentration C2 of the mixture of solution and snow liquid water is

(1)

At low concentrations, less than about 1.5 p. p.m., fluorescent intensity is directly proportional to solution concentration. At higher concentrations the dye solution may exhibit quenching or internal absorption so that the intensity-concentration relationship becomes nonlinear, and may not be monotonic. Once linearity is determined with a calibration curve (intensity versus concentration) the ratio of initial fluorescent intensity I1 to the final intensity I2 yields the ratio of the concentrations and the inverse ratio of the masses of solution:

(2)

The mass fraction of snow liquid-water content is

(3)

The volume fraction θw of liquid water in the snow sample with volume Vs is

(4)

where ρw is the density of water.

The freezing-point depression can be calculated for ideal dilute solutions (Daniels and Alberty, 1975, p. 130) as

(5)

where Kf is 1.86 deg mol−1 for water and M is the molal concentration (moles solute per kilogram of solvent). A dye solution concentration of 1 p. p.m., produces a freezing point depression of c. 4×10−6 deg.

Method

Rhodamine WT is the dye used in this study because it has a low minimum detectability, low photochemical decay, and low cost (Smart and Laidlaw, 1977). It is purchased as a concentrated solution, specified as 20% by weight. A dilute solution (1 p. p.m.) is prepared in the laboratory and then carefully measured into small vials, 100 g each. Some of the solution is saved for the measurement of initial fluorescent intensity.

A 500 cm3 snow sample is removed from the snow surface or a pit wall using a coring tool and a steel spatula, which have been kept at snow temperature by storage in the adjacent snow. The sample is weighed with a triple-beam balance, then put into the mixing container, a thin-wall stainless-steel wide-mouthed bottle that is immersed in an ice bath. The container is covered with an insulating lid between uses, and the mixture is stirred with a rod through the lid when the air temperature is warm. The ice bath can be maintained in a standard ice chest.

The pre-measured dye solution (m1 = 100 g) is brought to 0° C in the field, by placing the vials in the ice bath some minutes before measurement. The contents of a vial are poured over the snow sample, and the mixture is shaken and stirred for about 30s. A small amount of liquid (c. 5 ml) is extracted with a squeeze bulb and a pipette fitted with a fine screen on the end to separate the liquid from the ice grains. The sample is stored in a small bottle for later analysis.

A Turner Associates filter fluorometer, Model 110, was used for the data analysis. The filters used followed the recommendations of Smart and Laidlaw (1979), the primary using Corning 1–60 with Wratten 61 and the secondary Corning 4–97 with Corning 3–66. Possibly lower concentrations of rhodamine WT could be used if the fluorometer were more sensitive. The fluorescent intensity measurements require 3.5 ml of solution. Each sample is measured alternately with the standard.

Errors

Worst-case absolute errors in the measurement of the mass and volume liquid phase fraction are

(6)
(7)

where E is the relative error, defined as

(8)

Relative errors for the measurements of snow volume, snow mass, solution mass, and fluorescent intensity, with our apparatus, for snow densities between 250 and 650 kg m−3, are estimated at

Therefore

Errors in the liquid mass fraction xw and volume fraction θw are sensitive to E(I), the relative error in the fluorescent intensity measurement. If E(I) were reduced to 0.01, errors in xw and θw reduce to

Another possible error source is inadequate mixing of the dye solution with the snow sample. The error in xw increases with the amount of solution added (Equation (6), but if too little is added the resulting mixture is inhomogeneous. If too much is added, the dye dilution is too slight. Visual tests with concentrated dye solutions showed that 50–60 g are required to obtain adequate mixing.

Tests and Discussions

The technique was tested in a variety of field and laboratory conditions. Comparisons with other techniques have not yet been made.

For laboratory trials, large volumes of snow, 0.1 to 0.25 m3 at densities from 350 to 650 kg m−3, were sieved into a specially designed cabinet, with ice baths in the side-walls surrounded by insulating foam and a 0.20 m layer of fine sand in the bottom to reduce the thickness of the saturated basal layer. The fluorescent dye dilution method consistently gave zero water content for dry frozen snow of varying densities, demonstrating that the mixing process itself causes no melting. The snow was then partially melted by radiation and allowed to drain; a metal pan collected melt water. Measurements of snow liquid-water content in samples of various densities at field capacity were found to be in good agreement with those published by Denoth and others (1979).

In field trials the method seems easy to use and requires little training. The time required for snow sample removal from a pit wall, mixing, and solution sample extraction is about 5 min. Thus fluorescent dye solution appears to be a useful technique for the field measurement of snow wetness. Compared to alternatives, it is acceptably accurate, requires little field apparatus, uses only snow and water as a coolant, and is fast.

Acknowledgements

Dan Dawson of the University of California Sierra Nevada Aquatic Research Laboratory gave invaluable help. Ron Perla and Albert Rango made useful comments on an earlier draft of the manuscript. Funding was provided by NASA Grant NGT-803.

References

Bader, H. 1948. Theory of non-calorimetric methods for the determination of the liquid water content of wet snow. Schweizerische Mineralogische und Petrographische Mitteilungen, Bd. 28, Ht. 2, p. 35561
Bader, H. 1950. Note on the liquid water content of wet snow. Journal of Glaciology, Vol. 1, No. 8, p. 46667.
Colbeck, S.C. 1978. The difficulties of measuring the water saturation and porosity of snow. Journal of Glaciology, Vol. 20, No. 82, p. 189201.
Daniels, F., and Alberty, R.A. 1975. Physical chemistry. Fourth edition. New York, John Wiley and Sons Inc.
Denoth, A. 1979. Study of water drainage from columns of snow. CRREL Report (Hanover, N. H.) 791.
LaChapelle, E. R., and Perla, R.I. Unpublished. Wet snow revisited. [Paper presented at International Snow Science Workshop, Bozeman, Montana, 1982.]
Morris, E.M. 1981. Field measurement of the liquid-water content of snow. Journal of Glaciology, Vol. 27, No. 95, p. 17578.
Smart, P.L., and Laidlaw, I.M.S. 1977. An evaluation of some fluorescent dyes for water tracing. Water Resources Research, Vol. 13, No. 1, p. 1533.