Wet to dry growth regime transition

AH natural accretions observed in the present studies at temperatures below -8°C were of the dry type regardless of location on the blade or LWC, indicating that the blades were in the dry growth regime at windspeeds up to 150 m/s. In contrast, in our laboratory rotor experiments (Ackley and others 1979), complete dry growth conditions started only below -24 °C and at a LWC around I g/m³. Moist growth conditions in which liquid water exists but does not migrate were between -14 and -23°C. Experiments at higher than -14°C were entirely in the wet growth regime.

Lozowski and others (1979) observed dry growth conditions only at a temperature of -15°C, LWC 0.4 g/m³ and a wind speed of 30 m/s when no ice particles were added. With the addition of ice crystals of 0.1 to 0.3 g/m³ they claimed that the dry growth range expanded to -5°C for a LWC of 0.4 g/m³ and wind speed 92 m/s. However, the appearance of accumulated ice noted in their report indicated that the ice particles were collected on the wet surface.

Table 1.ICE RUN SUMMARY. NOTES; A: TEMPERATURES MANUALLY MEASURED; B; THICKNESS OF ACCRETED ICE ESTIMATED FROM BLADE PHOTOS; C: THICKNESS ESTIMATED FROM LASER PROFILER; D: TWO SPEED RUNS MADE CONSECUTIVELY.

Stallabrass and Hearty (1979) made a series of icing tests using the same icing wind tunnel as Lozowski and others (1979) but a different ice particle generator called a “snow nozzle”, which generated large numbers of minute ice particles having a median diameter of 15μm was used. The ice particles sprayed by the “snow nozzle” caused drastic differences in morphological aspects. Especially at lower wind speeds, the cross section became wedge-shaped. At higher wind speeds the cross section resembled a rather truncated wedge. Stallabrass and Hearty observed a dry growth regime at -15 °C, LWC 0.4 g/m³ and a wind speed 61 m/s without ice particles. judging from the photograph in their Figure 5, this condition may have been a moist growth regime. With the addition of ice particles of 1.0 g/m³, the dry growth rose to -5°C, for a LWC of 0.4 g/m³ and a wind speed of 30 m/s. Tests made at wind speeds higher than 30 m/s were all in the wet growth regime.

As discussed by Stallabrass and Hearty, concentrations of ice particles produced by their “snow nozzle” could not be oberved in the natural case. All wet growth regime results by Lozowski and others were under the comparable conditions of -8°C, LWC of 0.12 g/m³ without ice crystal or 0.28 g/m³ and ice crystal content (ICC) of 0.8 g/m³ at a wind speed 110 m/s. We observed pure dry growth regime under comparable conditions of -7.5°C, LWC of 0.5 g/m³ and maximum wind speed of 115 m/s. The amount of ICC was not measured in our studies and was expected to be widely variable, but even if an amount of ice particles comparable to that of Stallabrass and Hearty existed in the present studies, the wet to dry growth regime transition was at a much higher temperature under natural conditions than in the laboratory since wind speeds were much higher.

Several sources of discrepancies can be pointed out.

a) Temperature measurements in the present studies were made in natural fog but the sensor was protected so that little or no ice accretion occurred. Ambient temperature was used for the laboratory rotor experiments (Ackley and others 1979), and the real temperature in the fog was presumably much higher than the ambient temperature due to spraying warm water. Apparently Lozowski and others (1979) deduced the test section temperature from their plenum chamber temperature controller setting. One example given by them was a plenum temperature of +2.5 C, relative humidity (RH) of 90% and static pressure of 1013.25 mb, which would give -5°C at an air speed of 120 m/s at the test section. So great a temperature drop would increase RH to 195% over ice even without the introduction of any water drops. Possible supersaturation could lower the apparent transition temperature by either supplying more liquid water or raising temperatures by latent heat of condensation or both. The test section static temperatures for Stallabrass and Hearty’s tests were derived from direct measurements of dry tests, but problems similar to those that Lozowski and others encountered may still exist. Also rapid freezing of droplets from their “snow nozzle” could release heat, affecting the results.

The spray nozzle for Ackley and others was placed only 50 cm from the rotor so that droplets had little time to cool down and considerable vapor was generated from the warm droplets. There are many published icing studies but most give insufficient detail to estimate RH. For instance no detailed geometry was given by Laforte and others (1983). Considering the size and configuration of their cold room and wind tunnel, conditions similar to those of Ackley and others would apply. Such a humid environment may also exist in the Ottawa spray rig (Stallabrass 1958) since the rig uses steam to atomize water and releases extensive water vapor along with the droplets.

b) Liquid water supply under natural conditions, especially for all test systems used in the present studies, is close to the snow surface, and thus can be lower than the value obtained by multi-cyclinder measurements at the observatory tower about 20 m higher. Nearby snow surface and blown-up snow particles are a good vapor sink. Comparison between near-equilibrium natural conditions and highly transient laboratory test conditions of all four tests cited here seems difficult, but the water supply through the vapor phase in an icing wind tunnel can be much higher than under the natural conditions of the present studies.

Compared with the very large latent heat of freezing, the heat content of droplets only few degrees higher than ambient temperature would cause little change in wet to dry growth transition temperature. However, supersaturation of vapor caused by evaporating warm cloud droplets (as in the laboratory environment) could supply a large amount of water and also cause some temperature rise. Calculations made by Lowell (1953) indicated that the vapor supply from individual droplets is small for small obstacles, but continuous flow of a large number of droplets could provide a significant water supply through the evaporation and condensation process. Frequently we observed crystallographic (high faceted) surfaces especially near the edge of the accretion, indicating a vapor growth condition existing at that location.

Droplet Capture Efficiency Index (DCEI)

In order to compare data given by various authors certain common measures have to be devised. Probably a quantity (amount of captured water/amount of supply) could serve reasonably well as such a measure. Let us call this quantity the droplets capture efficiency index (DCEI). Of course DCEI is a function of various parameters such as incoming droplet size distribution and air velocity, geometry and material of the collecting structure, as well as supply rate and temperature. Since we measure the rate of thickness increase R_c DCEI (E_i) can be defined as

(1)

where V is air velocity, W is LWC, and ρ is the density of accreted ice. The density of accreted ice is fairly close to 0.9 g/cm² under the high-speed impact conditions found in the most parts of the present blade. Velocity V can be calculated from rotor RPM and radial location of the accretion. The same definition can be applied to similar types of measurements which measure thickness growth rate (Stallabrass and Hearty Hearty, and Lozowski and others). Some measurements, such as those of Bain and Gayet (1982), were expressed by the rate of cross-sectional area increase. We have to be content with an average growth rate by assuming that the collection area stays constant. In Figure 2 DCEI calculated from present field observation data are plotted together with those of Lozowski and others, Stallabrass and Hearty, and Bain and Bayet. Also some of our laboratory rotor experiment results, partly published by Ackley and others, part in oreoaration by Itagaki and others are shown by vertical lines indicating the range of DCEI. Since DCEI differs depending on the radial location on the rotor, only the range is shown. Examples of the radial distribution of DCEI obtained from our laboratory rotor experiments are shown in Figure 3. The laboratory rotor results cover the range of DCEI calculation from data given by Lozowski and others. Extensive ice crystal injection seems to have shifted higher temperature points of Stallabrass and Hearty considerably. Their lower temperature points and higher temperature without ice crystal injection seem unaffected, and agree with Itagaki and others and Lozowski and others. Although the points are scattered widely, several features can be pointed out.

Fig. 2.Droplet capture efficiency index (DCEI) calculated from various reports as a function of temperature, results indicated that icing wind tunnel study DCEIs are higher than those under natural icing studies.

• 1) Present measurements give the lowest DCEI of all other measurements.

• 2) DCEI calculated for natural icing measurements of aircraft by Bain and Gayet, especially with ice particle counts C_i higher than 5/L, are much lower than those of the laboratory rotor icing by Itagaki and others, and the icing wind tunnel studies by Lozowski and others, and Stallabrass and Hearty.

Two possible causes contributed to the lower DCEI for the present studies. The abundant supply of ice crystal is one. As shown in Figure 2, the regression line for Bain and Gayet of high crystal count of C_i (they arbitrarily set it at 5/L) especially at higher temperatures, is much lower than the all-inclusive line, indicating that high ice count is a major factor contributing to lower the present DCEI. However, no further lowering trend of DCEI for C_i higher than 5/L can be observed in the results by Bain and Gayet, indicating that a further reduction mechanism is involved in our results. The other factor of lower DCEI is the centrifugal force field and air flow in the radial direction along the high speed rotor blades. As shown in Figure 3, DCEI measured in laboratory conditions (Itagaki and others) gradually drops by an increase in radial location of the blades beyond the disturbed area near the hub. According to Langmuir and Blodgett (1946) collection efficiency E_M is a function of K and Φ, and both are proportionally increased with velocity U. Although φ tended to reduce E_M, higher values of K cause an increase in ?_? as a whole within the range of the present study. Overall, an increase of DCEI with an increase in U is expected from Langmuir and Blodgett’s theory. This result is an opposite trend to that found in rotor experiments since rotor blades encounter higher wind speed with an increase in radial location of the blades.

Fig. 3.Radial distribution of DCEI of wet, moist, and dry conditions obtained from laboratory studies showing the effects of centrifugal acceleration and radial air flow caused by rotation of the rotor (Itagaki and others, to be published).

Two possible causes could contribute to this discrepency. Centrifugal acceleration would be especially effective in moving free water in wet growth condition. Since radial components of air flow are combined with the normal component of oncoming to blade surface, droplets carried by the air flow do not impinge the rotor blade perpendicularly, reducing the collection efficiency. A gradual drop in DCEI of dry growth case may be mainly caused by such a mechanism.

Humps in the curve appearing around the 15-cm radius for the moist growth case may be caused by the outward motion of migrating water. More active migration of water in the wet case may help to shed water, causing DCEI to be actually lower than in the moist case. Because most of the natural icing rate was measured near the tip, any of the reducing mechanisms would make DCEI much lower than in the nonrotating case. Present results seem to agree reasonably well after such adjustment, with Bain and Gayet having a C_i higher than 5/L.

Morphological aspects

The laser profile camera was used on eight icing runs and thin section studies were made in six runs. At higher temperatures and wind speeds, Lozowski and others, and Stallabrass and Hearty observed that accretion extended more than 90e from wind direction along the cylinder surface. However, in the natural icing in the present study, the extent of accretion on the cylinder blades stayed within ±60° from the stagnation lines along the cylinder, with a pronounced hump along the edge of accretion for even the most severe case (run 13). A few cone-shaped grains were found beyond the edges. Contrary to the rather moderate icing Found on the cylindrical blades, accretion on the airfoil blade has a flat-nosed rough profile outside the 40-cm radius. Such a cross section would greatly degrade the performance of a rotor or propeller. It appears that the two humps found on the cylindrical blade were merged, eliminating the flat smooth part due to the small radius on the airfoil blades. If such merging of humps takes place, simple modeling using a certain scaling law may not be applicable (Armand and Charpin 1976).

Runs number 7, 12 and 15 were in slightly wet or moist growth regimes and small humps appeared but we never encountered the type of accretion described by Stallabrass and Lozowski (1978) as a “thin cornice4ike sheet” nor did we observe the “mushroom-double-horn” observed by Laschka and Jesse (1978). Probably ice of weaker mechanical strength could not survive under the dynamic conditions found in the rotor experiments. As discussed in previous papers (Itagaki 1983a, b) such accreted ice would shed before reaching a thick protrusion.