Background

Radar-based snow property retrieval exploits subtle changes in backscatter resulting from variations in accumulation and metamorphosis to derive snowpack information without physical contact. In terrestrial environments, a simple conceptualization of total backscatter (σ ^tot) can be made with snow- and soil-scattering contributions in a particular transmit-and-receive polarization combination (pq) (Ulaby and others, 1984; Reference RottRott and others, 2010):

where the air/snow interface (σ ^as), snow/ground interface (σ ^gnd), snow volume (σ ^vol) and higher-order interactions among the ground and snow volume (σ ^gv) contribute to total backscatter (Fig. 2). The magnitude of each contribution in Eqn (1) is determined by the dielectric and physical state of the snow-covered environment and the parameters of the observing instrument. With parameters of the observing instrument held constant, spatio-temporal changes in SWE can be expected to exert influence on backscatter because of its inherent relationship with both physical and dielectric properties of the snowpack.

Fig. 2.

Left: set-up of UW-Scat, illustrating first-order backscatter for snow-covered terrain (adapted from Reference RottRott and others, 2010). Right: composition of theoretical single-layer Ku-band scattering contributions for a snow-covered tundra environment (modelled with the QCA/ DMRT implementation of Reference Tsang, Pan, Liang, Li, Cline and TanTsang and others, 2007). Model input parameters: f = 17.2 GHz, ε _r,_gnd = 5 + 0.5i, ρ = 250 kg m⁻³, d = 1 mm, τ = 0.1 and θ = 40°. Observed range of depth shown in grey.

Dielectric properties of target media are commonly described using the complex form of relative permittivity ε _r:

where the real component ε′ describes the ability of a material to polarize and store energy and the imaginary component ε″ is a loss factor describing dissipation of energy, both relative to that of air. For dry snow, values of the imaginary component of permittivity are generally low at microwave frequencies (ε′ < 2 and ε″ < 10⁻³), resulting in negligible absorption of incident energy, dominant scattering losses, and potential for penetration through meters of snow. If the observed snow becomes wet, the presence of liquid water causes increased reflectivity at the snow surface (ε′ ≈ 20−80), greatly increased attenuation within the snow volume ( ε′ ≈ 5−40) and, therefore, diminished potential to retrieve snow properties at microwave frequencies.

Incident energy from a ground-based radar system directed towards a dry snowpack interacts first at the air/ snow interface, where it is partially reflected in different directions and partially transmitted into the snowpack. The magnitude of each component depends on the dielectric mismatch between the surface media and air, the roughness at the interface, and the geometry of the radar. In the case of dry snow, the vast majority of incident energy propagates into the volume at incident angles greater than nadir (θ > 0) because of the small difference in permittivity between the air (ε′ ≈ 1) and the snow (ε′ ≈ 1.05−2). Assuming a smooth surface, incident energy reflected at the air/snow interface can be estimated using the square of the Fresnel reflection coefficients, where if and θ = 40^°, only 5.9% of the horizontally polarized and <1.0% of the vertically polarized incident energy is reflected. As a result, σ ^as is generally considered to be a minor contributor to dry snow backscatter and is often neglected.

Within the snow volume, variability in σ ^vol results from changes in physical properties including depth, density and microstructure (Reference FungFung, 1994; Reference Tsang, Pan, Liang, Li, Cline and TanTsang and others, 2007; Reference Du, Shi and RottDu and others, 2010). As a mixed medium, dry snow consists of ice crystals in an air background, with ice structures contributing volume scatter at microwave wavelengths. As depth increases, the path length of the propagating wave is extended, increasing the potential for scattering within the volume. A theoretical 17.2 GHz response to increasing depth is demonstrated in Figure 2, where when the quasi-crystalline approximation/dense-media radiative transfer model (QCA/ DMRT) of Reference Tsang, Pan, Liang, Li, Cline and TanTsang and others (2007) is parameterized with conditions common to tundra environments, co- and cross-polarized σ ^vol is found to increase by >10 dB with depths up to 1 m. Open tundra observations in Churchill span a relatively limited range of the demonstrated sensitivity, which coincides with strong increases in σ ^vol as depth departs from 5 cm. Snow density (ρ) contributes to σ ^vol through variation in the number of scatterers, and consequently the permittivity and the extinction coefficient of the snow volume. A functional relationship exists where ε′ = 1 + 0.0019ρ, independent of frequency in the microwave spectrum (Reference Hallikainen, Ulaby and AbdelrazikHallikainen and others, 1986). According to this relationship, seasonal snow occupies a narrow range of ε′ between approximately 1.19 and 1.70 (100 and 400 kg m⁻³). Despite the limited range, variation in snow permittivity resulting from seasonal and spatial changes in density can contribute internal reflections and therefore influence σ ^vol. Higher-order interactions contributing to σ ^vol are often difficult to quantify, as complexity of the signal is exacerbated by seasonal accumulation and metamorphosis which drive intricate layering, thereby evolving vertical and horizontal heterogeneity of scattering within the snowpack.

The influence of snow metamorphosis on radar response is dictated by a complex set of interactions controlled by grain size, grain shape and aggregate structure. In the case of seasonal snow, processes of vapour transport and subsequent grain growth can exert significant influence on volume scatter as the ratio between grain diameter and wavelength (d/λ) is increased. This relationship is classically defined by Rayleigh scattering theory where scattering is proportional to the fourth power of frequency and the third power of size. In practical application, dependence on grain diameter alone does not account for real-world variations in shape and aggregate structure that may contribute significant portions to observed scatter in addition to multiple scattering between densely packed grains. For example, Reference Du, Shi and RottDu and others (2010) suggest that as the ratio between the long and short axis of a theoretical ellipsoid grain is reduced, cross-polarized response may increase in low to moderate snow volume-scattering environments (i.e. increased depolarization with prolate-shaped grains in shallow snow environments). Similar observations have been made in field studies such as Reference Yueh, Dinardo, Akgiray, West, Cline and ElderYueh and others (2009) where a strong seasonal depolarization response was attributed to the development of non-spherical depth-hoar grains. In addition to grain shape, recent studies have suggested that bonding and evolving microstructure can play an important role in observed scatter where aggregate grain structures contribute stronger effective scattering than their individual constituents (Reference Tsang, Pan, Liang, Li, Cline and TanTsang and others, 2007; Reference Chang, Tan, Lemmetyinen, Tsang, Xu and YuehChang and others, 2014). Given the potential for dynamic grain growth (0.5 mm > d < 6 mm) and development of aggregate depth-hoar structures, it can be expected that metamorphosis of the observed open tundra snowpack will be a notable contributor to the volume-scattering response in addition to bulk properties such as depth or SWE.

If incident microwave energy successfully traverses the snow volume, it is subjected to reflection at the ground surface. Unlike σ ^as, spatio-temporal variability in σ ^gnd is common in terrestrial dry snow environments, where local surface properties can exert influence on total backscatter due to the larger dielectric contrast of the surface media (ε′ > 3) and typically large standard deviation of surface height relative to the wavelength (h >λ/ 32 cos θ; Ulaby, 1981). Soil moisture and state play an important role in determining reflection where a larger portion of incident energy may be returned into the snow volume when soil is moist and ε′ is elevated. Seasonally, this is an important consideration when accumulation occurs before the soil has frozen and free moisture is present. Spatially, variation in surface scattering generally results from differences in surface roughness, soil and vegetation type, and heterogenous soil moisture patterns. In general, σ ^gnd can be expected to contribute less to total backscatter than σ ^vol at Ku-band in snow-covered tundra environments (Fig. 2). Energy reflected back into the snowpack may again scatter within the volume and/or scatter within volume followed by reflection from the ground surface, generating higher-order scatter contributions (σ ^gv).

Backscatter measurement

To characterize backscatter response, a frequency-modulated continuous wave radar system known as the University of Waterloo scatterometer (UW-Scat) was deployed (Reference King, Kelly, Kasurak, Duguay, Gunn and MeadKing and others, 2013). Pulled by snow machine, the Ku-band unit of UW-Scat was transported in a sled-based configuration to terrestrial locations and configured to collect backscatter measurements over a 15 m × 20m area in <20 min. In the microwave remote sensing of snow, choice of frequency is often a compromise between penetration depth and sensitivity to desired snow properties. At Ku-band (12–18 GHz), the corresponding wavelengths are able to penetrate dry snow to depths >1 m (Reference MätzlerMätzler, 1987; Reference Marshall, Koh and ForsterMarshall and others, 2004). For the purpose of observing tundra-class snow, Ku-band was therefore sufficient to penetrate the expected range of depths (0.10–0.75 m; Reference Sturm, Holmgren and ListonSturm and others, 1995). Moreover, the proximity of the observing instrument wavelength to the scale of individual snow grains was close enough to solicit a large volume response without saturating within the upper bounds of the snowpack. Backscatter measurements made with UW-Scat were collected at a centre frequency of 17.2 GHz across a narrow bandwidth of 0.5 GHz. From the sled-mounted position, the antenna and radio-frequency (RF) hardware operated at a height of ∼2.0 m with a narrow beamwidth of 4.3°. The resulting ground-projected radar footprint was <30 cm in azimuth and range directions. Additional operational parameters of use during the experiment are listed in Table 1.

Table 1.

UW-Scat operational parameters

Once an observation site was selected, the scatterometer was levelled to the local terrain and RF hardware was allowed to stabilize at 35°C to minimize temperature effects on the hardware. A two-axis positioning system was then used to direct the radar antenna hardware through a series of azimuth sweeps to collect measurements at elevation angles between 30° and 45° in 3° increments. Measurements at each elevation angle were integrated over a 60° azimuth sweep to improve the number of independent samples and ensure an adequate signal-to-noise ratio. In post-processing, the backscattering coefficient, σ ⁰, was estimated to express the ratio of power reflected to power transmitted as normalized to the ground-projected radar footprint. Copolarized vertical , horizontal and cross-polarized backscatter coefficients were derived based on the averaged range profiles and system geometry. Detailed discussion of signal-processing procedures can be found in Reference Geldsetzer, Mead, Yackel, Scharien and HowellGeldsetzer and others (2007) and Reference King, Kelly, Kasurak, Duguay, Gunn and MeadKing and others (2013).

To calibrate the scatterometer system, an accompaniment of internal and external procedures was used. Prior to each site scan, a trihedral corner reflector was erected in the field of view and observed to collect a short time series of measurements. Differences between the observed polarimetric measurements and reference target backscatter were corrected offline using a procedure described by Reference Geldsetzer, Mead, Yackel, Scharien and HowellGeldsetzer and others (2007). To characterize system and platform noise, open sky measurements were collected after each corner reflector measurement. Sky measurements were coherently subtracted from target range profiles to reduce the influence of system noise and isolate the desired target signal. Estimates of worst-case measurement error from the post-processing procedure were, on average, ±2.0 dB including a 0.5 dB addition for random error. In general, the observed errors were a function of the limited number of independent samples collected under the beam-limited conditions of the sled-based configuration as well as bias introduced by human and environmental inaccuracies with misestimation of the deployed sensor height and wind buffing of the reference target. A detailed discussion of the error estimation process can be found in Reference King, Kelly, Kasurak, Duguay, Gunn and MeadKing and others (2013).

Snow measurements

Destructive sampling within the scatterometer field of view was completed immediately after each scan to gather information about local snow properties and to evaluate snow variability at the sub-scan level. A standard procedure was used where horizontal heterogeneity in depth, density and SWE was quantified in addition to point measurements of vertical snow properties. On completion of the scatterometer measurement, a 15 m × 20 m box was measured within the field of view of the scatterometer to bound a snow-sampling area (Fig. 3). Within the sampling area, a grid of snow depth measurements was collected using a GPS-enabled Snow-Hydro MagnaProbe. Each grid contained a minimum of 200 measurements spaced across several transects parallel to the scatterometer range direction. Pairs of snow-core measurements were also collected at six locations within the sampling area to estimate bulk density and SWE. The snow-coring instrument had a cross section of 30 cm² and is often referred to in the literature as the ESC-30 (Reference Pomeroy, Marsh and GrayPomeroy and others, 1997; Reference DerksenDerksen and others, 2012; Reference Rees, English, Derksen, Toose and SilisRees and others, 2014). Using a handheld spring scale, the weight of each snow core was recorded, along with the depth at the measurement site.

Fig. 3.

Destructive snow-sampling protocol plan view. At each site a distributed set of bulk and stratigraphic measurements was made to quantify variability within the scatterometer field of view.

In addition to bulk snow measurements, two snow pits were excavated at 3 and 5 m outwards from the scatterometer using standardized procedures (Reference FierzFierz and others, 2009). Multiple snow pits were completed to avoid mischaracterization related to pit placement and large variations in topography (e.g. hollows between hummocks). Once excavated, structural and textural discontinuities were used to define and record layer locations, thickness and general composition. A snow sample from each layer was extracted and placed on a grid comparator card for visual analysis. Using a stereo-microscope, grain origin types were identified and estimates of axial diameter were recorded. Density within each snow pit was measured along two continuous vertical profiles extracted from the pit face using a 100 cm³ box-style cutter and digital scale. Temperature profiles were constructed using a string of thermistors inserted into the snowpack with a vertical spacing interval of 4 cm.

Trench measurements

To evaluate the influence of lateral heterogeneity on backscatter, detailed measurements of snowpack stratigraphy were excavated within the scatterometer field of view. Following a protocol detailed by Reference Tape, Rutter, Marshall, Essery and SturmTape and others (2010), a 5 m trench was dug ∼3 m outwards from the scatterometer across the azimuth look direction to correspond with scatterometer measurements collected at elevations between 30° and 45°. The excavated face was prepared manually with hand tools to create a flat surface perpendicular to the ground surface. Once prepared, 850 nm centre frequency NIR photography was completed along the length of the trench using a linear rail system to maintain a constant distance to the trench face. Sequential photographs taken along the length of the trench were georeferenced using an in-scene cm-scale measuring staff positioned horizontally above the trench face. A single continuous image was stitched together from the collected set of photographs, and stratigraphy was manually extracted at a 1 cm horizontal resolution (Fig. 4). In addition to NIR photography, inter-layer snow properties were characterized with a set of five snow pits completed at 1 m intervals along the trench. Vertical transects of density, temperature and grain size were measured using the previously described standard snow-pit protocol.

Fig. 4.

A series of 850nm NIR photographs taken along the length of an excavated 5 m snow trench. Photographs were referenced and stitched together for analysis. Black lines show manually identified snow stratigraphy.

Seasonal and spatial snow properties

Accumulation within the Churchill study area evolved with spatio-temporal complexity related to variations in vegetation, topography and climate. Given the selected land-cover composition of flat open terrain and dominant graminoid vegetation, observation sites were exposed to a common set of sub-arctic environmental agents including strong wind and sustained low air temperature. The majority of accumulation within the study area was deposited between December and January, with a limited number of precipitation events occurring thereafter. In the observed open areas, snowpack development was heavily influenced by sustained winds, where average speeds commonly exceeded 5 m s⁻¹, rapidly redistributing accumulated snow. Mean snow depth at the observed tundra sites was shallow, ranging from approximately 4 to 25 cm, generally increasing through the season (Table 2). Examples at the extreme of this range were associated with changing land-cover characteristics found in close proximity to the observation site (e.g. forest transition zones situated near sites 14 and 15). Inter-site standard deviation of snow depth ranged between 20% and 64% of the mean, in most cases declining with increasing depth (R = −0.5, n = 26; correlations and coefficients of determination were significant at the 0.05 level). At the open tundra sites, microtopographic elements, including hollows between hummocks, trapped early-season snow and created deviations by up to double the inter-site mean. The influence of these features on total depth was reduced as accumulation increased relative to variations in surface height, effectively masking the smaller ground features. Despite the sustained influence of wind, bulk snow density remained low (<250 kg m⁻³) and did not vary substantially through the season. Compared to depth, inter-site variability of density was smaller at a majority of sites, with standard deviations accounting for 9–46% of the mean. As a product of depth and density, the observed range of SWE was seasonally and spatially limited to 70.0 mm or less. At the tundra observation sites, variation in SWE showed a stronger linear relationship with depth (R ² = 0.98) than density (R ² = 0.46) as a result of the smaller range of bulk density encountered.

Table 2.

Inter-site snow properties measured at each tundra observation site. Dates of observation are presented as day of year (DOY) spanning the 2010/11 observation period. Bulk SWE and density measurements were not available on DOY 60

Snow stratigraphy excavated within the scatterometer field of view increased in complexity from an early point in the experiment. Sequential periods of accumulation and wind transport created two to seven distinct horizontal layers of varied thickness and texture. A basal depth-hoar layer was the most consistent feature excavated among the open tundra sites. In the 50 pits completed, depth hoar comprised, on average, 52% of total depth. The rapid development of the basal hoar layer was driven by a sharp early-season decline in air temperature sustained through the end of the experiment with limited increases in depth. Vertical temperature gradients measured through the shallow snowpack exceeded 20°C m⁻¹ in 40 of 50 open tundra pits, a strong indicator of sustained kinetic growth. Well-defined cups were a common feature of the basal depth-hoar layer, with large aggregations present from DOY 334 onward. By the end of the observation period, grains within the depth-hoar layer had exceeded 3 mm in major axis diameter, with poly-aggregates reaching 6 mm or larger (Fig. 5). Thickness of the basal depth-hoar layer was heavily influenced by inter-site changes in ground surface height. As a result, the thickness of the basal hoar layer between intersite snow pits was found to vary by up to 10 cm where periodic hummock features were present.

Fig. 5.

Basal depth hoar at site 25 on a 2 mm grid comparator card. The large aggregations found at site 25 were common to most observation sites from DOY forward.

Contrasting snow surface features were heavily influenced by wind transport, featuring multiple slab layers separated by hard thin crusts. Grain diameter within the surface slab layers was generally small (<1 mm) due to persistent wind action and subsequent rounding of grains with transport. A vertical gradient of grain diameter became apparent in the latter part of the experiment, where wind-rounded grains transitioned into solid facets with sustained temperature gradient metamorphosis. In several of the late-season snow pits, large faceted grains were found intermixed all the way to the surface of the snowpack. Few ice features were identified, with those found being very thin snow-ice layers situated at the base of the pack from early-season melt processes. Rapid redistribution of snow accumulation limited the number of fresh-snow observations collected during the experiment; in most cases, surface layers identified with fresh snow were <2 cm thick and intermixed with wind-rounded grains.

Overall, the rapid and often subtle changes within the shallow tundra snowpack provided a challenging target of analysis and a unique opportunity to evaluate distinctive features previously unaddressed at Ku-band. The predominant local processes of wind redistribution and temperature gradient metamorphism were characteristic of conditions previously described along the Hudson Bay coast and of general conditions present with tundra-type snow (Reference Sturm, Holmgren and ListonSturm and others, 1995; Reference Kershaw and McCullochKershaw and McCulloch, 2007; Reference King, Kelly, Kasurak, Duguay, Gunn and MeadKing and others, 2013). Electromagnetically, the early and rapid development of large depth hoar had the potential to drive strong increases in backscatter as seasonal and spatial processes of accumulation and metamorphosis progressed.

Comparison of backscatter measurements and snow properties

To evaluate spatio-temporal backscatter sensitivity, snow property measurements collected at each site were compared against coincident estimates of σ ⁰. In an effort to reduce the influence of sub-scan variations in microtopography, estimates of σ ⁰ were averaged to integrate a number of azimuth sweeps across a small range of incident angles between 30° and 45°. In the averaged scatterometer measurements, the dynamic range of σ ⁰ was found to be >8 dB. Co-polarized and ranged in magnitude from approximately –13 to –5 dB while cross-polarized and responses were measured across a lower and smaller range between –26 and –15 dB. For the entirety of the experiment period, cross-polarized and were found within 0.1 dB and therefore were considered reciprocal for the purpose of analysis.

The observed relationships between depth, SWE and σ ⁰, as shown in Figure 6, indicate Ku-band sensitivity to evolving snow properties at the 26 open tundra sites. Across the small range of encountered depth, a clear linear relationship with emerged, where vertically polarized backscatter increased by ∼0.22 dB for every 1 cm increase in depth (R ² = 0.67). A slightly less sensitive response, not shown in Figure 6, increased by 0.17 dB for every 1 cm in depth (R ² = 0.44). The observed sensitivity agrees with the theoretical relationship demonstrated in Figure 2, where increasing path length generates a strong volume response in shallow snow with large grains (>1 mm). Preferential vertical scattering was apparent throughout the experiment, where 18 of 26 observations demonstrated a co-polarization ratio less than 0. The Ku-band co-polarization ratios were moderately correlated with the number of layers observed within the scatterometer field of view (R = −0.64) suggesting that rough surface interactions within the layered accumulation played a role in the observed horizontal response. Alternatively, it is possible that the observed vertical arrangement of depth-hoar aggregates along the path of vapour transport contributed to the stronger vertical response. The cross-polarized response was comparable in slope to the co-polarized, increasing by ∼0.17 dB for every 1 cm increase in depth (R ² = 0.39). The coevolution of the co- and cross-polarized response was reflected in a small standard deviation of the depolarization ratio , where was generally 9–14 dB lower than . The strong cross-polarized backscatter is indicative of multiple scattering between density-packed grains and/or the presence of non-spherical snow grains (Reference Tsang, Pan, Liang, Li, Cline and TanTsang and others, 2007; Reference Yueh, Dinardo, Akgiray, West, Cline and ElderYueh and others, 2009; Reference Du, Shi and RottDu and others, 2010).

Fig. 6.

Comparison of a ⁰ averaged for incident angles between 30° and 45° against snow depth (a) and SWE (b) at each tundra observation site. Solid circles show response, and hollow circles show response. Measured and responses not shown, to improve readability.

Similar to snow depth, spatio-temporal variation in SWE was limited by persistent wind action and negligible precipitation input. Despite this, the observed increase in σ ₀ was large relative to the small range of observed SWE. Sensitivity to SWE was strongest with , increasing by 0.82 dB for every 1 cm in SWE (R ² = 0.62). Similar to the observed relationship with depth, showed a lower but significant sensitivity to SWE at 0.62 dB for every 1 cm increase (R ² = 0.42). Finally, the cross-polarized sensitivity was observed at 0.80 dB for every 1 cm increase in SWE (R ² = 0.36). In the relationship between SWE and σ ⁰, backscatter diversity often separated sites of similar aggregate composition, in some instances by several decibels. This finding highlights the complexity of the observed interaction space, where density, grain size and vegetation/ soil properties are important contributors to backscatter in addition to variation in depth. Seasonality and metamorphic state of the snowpack appeared to play a role in the observed backscatter diversity where increases in the major axis diameter of grains measured with a grid comparator card were moderately correlated with increased vertical backscatter (R = 0.39). The identified relationship with grain diameter was not found to be significant with horizontal or cross-polarized backscatter. While this finding is of interest, the seasonality of the measurements and, as a result, covariance of depth and grain growth made it difficult to decompose causation between the evolving snow properties. Moreover, the previously demonstrated spatial variability in stratigraphy made it extremely difficult to interpret the inter-site snow pits in the context of the larger scatterometer field of view. Overall, the distributed measurement protocol was able to identify Ku-band sensitivity to bulk snow properties when both in situ measurements and radar observations were averaged up to the site scale, but did not provide the means to quantify the role of stratigraphy, grain size and surface properties in observed backscatter diversity.

Evaluation of trench backscatter response

Direct comparison of in situ sampled snow properties and σ ⁰ revealed Ku-band sensitivity to increasing snow volume. Despite the positive result, snow pits completed within the scatterometer field of view yielded insufficient information to evaluate the influence of sub-scan lateral heterogeneity on observed backscatter. To address this open question, two 5 m trench experiments were completed on 7 and 8 January to characterize variation in stratigraphy within the scatterometer field of view. Collocated radar returns measured across the azimuth range of the scatterometer were compared with excavated snow stratigraphy to evaluate potential sub-scan influences on backscatter. The first trench was excavated in an open area adjacent to a transition zone, hereafter referred to as the forest edge site. The forest edge site possessed snow features common to the previous open tundra sites including limited depth, predominant windslab/depth-hoar composition and a rough underlying ground surface. The second trench was completed within a sparsely populated tree stand where the sheltered snowpack was composed of a larger number of lower-density layers. Comparison of the two targets provided an opportunity to evaluate a range of snow conditions and their influence on backscatter at scales local to the observing instrument.

A complex arrangement of internal layers with several discontinuous features was observed at the forest edge site (Fig. 7a). Within the shallow snowpack, three to five distinct layers were found at any given horizontal position, and, in total, six unique layers were identified. Total snow depth along the trench varied between 16.4 and 37.2 cm with a standard deviation of 5.6 cm (Fig. 7b). The observed variation in depth was in agreement with intersite measurements completed at the previous open tundra sites, where large changes in total depth were encountered over short distances. The most prominent change in snowpack composition was associated with a protruding hummock feature centred at the midpoint along the trench. Prior to excavation, the smooth surface of the mid-season snowpack provided no indication of the heavy influence of this feature on both total depth and stratigraphy.

Fig. 7.

Stratigraphy (a), depth (b) and relative backscatter (c) observed along the length of the forest edge trench. Layer notation in (a) corresponds to description in Table 3.

Internal stratigraphy of the forest edge snowpack consisted of several wind-influenced features underlain with a continuous layer of depth hoar (Table 3). A number of thin wind crusts (<0.5 cm), harder in texture than the surrounding snow, separated the larger internal layers of the snowpack. The upper and most recent feature, noted as layer 6 in Figure 7, was a smooth continuous surface layer composed of small wind-rounded grains intermixed with decomposing needle-like precipitation (0.1–0.4 mm). Beneath layer 6, a set of thin soft slabs, noted as layers 4 and 5, surrounded the apex of the prominent hummock feature where wind scouring had created a notable horizontal discontinuity. Each slab was composed of slightly larger wind-rounded grains (0.4–1.0 mm) and was similar in density to the surface slab layer (220 kg m⁻³). The largest continuous feature identified within the trench was a mixed-type layer composed primarily of faceted grains identified as layer 3. Within this large continuous layer, a wide range of grain size was found (0.2–1.5 mm). On the right-hand side of the trench, a hard relict wind slab was identified as layer 2 (3–5m) in which densities were the highest within the snowpack, increasing to ∼280 kg m⁻³. The basal surface of layer 5 was composed of high-density indurated hoar with well-developed cup structures >1 mm in diameter. Finally, the basal depth-hoar layer, noted as layer 1, contained striated cup-shaped grains and large poly-aggregates ranging in diameter from 1 to 4 mm. As a fraction of total depth, the depth-hoar layer composed on average 33% or 9.0 cm of the snowpack (Fig. 8b). The thickness of the basal layer was controlled by the ground surface height and location of the buried hard slab.

Table 3.

Description of stratigraphy excavated at the forest edge site. Layer numbers correspond to Figure 7

The excavated trench revealed an interesting target for radar observation where large changes in snowpack properties were found over short distances. Radar measurements collected as part of the forest edge scan were processed as individual returns relative to response of the collocated corner reflector and given approximate horizontal positions in relation to the trench face (Fig. 7c). As a general limitation of the observation protocol, uncertainty in the estimated horizontal radar position was greatest near the edges of the scan due to the arc of ground projected scatterometer sweep. The measured co-polarization response across the trench showed variability in relation to changing snow and soil conditions. In particular, variability was noted in relation to the previously identified hummock feature where co-polarized vertical backscatter decreased by 16% relative to the deeper accumulation situated at horizontal positions to the left of the feature. The horizontal backscatter response to the large change in snow depth was muted in comparison, emulating previously observed behaviour of the low co-polarization ratio observed in the distributed set of tundra snow targets. Across the width of the trench, co-polarized horizontal response was found to be ∼12% lower then the vertical response. To the right of the hummock, backscatter increased, reaching a trench maximum near the horizontal position of 3 m. The rapid increase in co-polarized backscatter coincided with increasing snow depth and complexity in layering. In particular, layer 5 was a unique dielectric and geometric discontinuity where the indurated depth hoar was both of higher density and larger grain size compared to the surrounding layers. Coupled with the increased depth to the right of the hummock, there was potential for multiple scattering, which appeared to be supported by the increased depolarization. Overall, the forest edge trench demonstrated the presence of dynamic changes in snowpack structure over short distances, which appear to have had a large influence on backscattered energy.

The second trench was completed within a sparsely populated tree stand, sheltered from strong local winds. Total depth along the trench ranged from 30.0 to 51.6 cm, with a smaller standard deviation of 3.1 cm. The contrasting influence of the local environmental agents was evident in the excavated stratigraphy (Fig. 8). Here layers were comparatively homogeneous, greater in number and, in most cases, found continuously through the 5 m trench. In total, nine unique layers were identified, with five present across the entire trench (Table 4). As in the previous excavation, a number of thin crusts (<1 mm) were found separating the major internal layers. Fresh precipitation, identified as layer 9, was the most recent layer and was composed of a combination of large stellar plates (1 mm) and much smaller graupel (0.1 mm). Below the fresh snow surface, a decomposing precipitation layer was found with smaller round grains (layer 8). Lacking influence from local wind, the two most recent layers were very low in density, ranging from approximately 100 to 150 kg m⁻³. The remaining layers of the snowpack were heavily influenced by temperature gradient metamorphosis, with grain size increasing towards the base of the snowpack. Layer 7, the more recent of two mixed-type layers, was composed of smaller rounded grains with some larger faceted grains (0.3–1.0 mm). A similar mix of grain types was found in layer 6, with a bias towards larger faceted grains (0.6–1.8 mm). Density increased within the more mixed layers, reaching a maximum of 270 kg m⁻³. Again, basal depth-hoar features dominated the remainder of the snow-pack, with layers 4 and 5 composed of large cup-shaped grains up to 4 mm in diameter. Density within the unconsolidated depth-hoar layers was lower, at ∼170 kg m⁻³. A number of discontinuous icy hoar features, identified as layers 1, 2 and 3, were found at the base of the pack. These thin features were very hard in texture and were composed of large grains up to 4 mm in diameter.

Fig. 8.

Stratigraphy (a), depth (b) and relative backscatter (c) observed along the length of the forest trench. Layer notation in (a) corresponds to description in Table 4.

Table 4.

Description of stratigraphy observed along the length of the forest trench. Layer numbers correspond to Figure 8a

Compared to the forest edge trench, the backscatter response from the forest trench was stable across the scan. The reduced variability in the co- and cross-polarized backscatter corresponded well to reduced variation in snow depth and increased homogeneity of the internal stratigraphy relative to the previous trench. In clear contrast to the forest edge site, there was no observed preference in orientation of the co-polarized backscatter. This observation separates the forest response from the open tundra sites where vertical preferential scattering was consistently observed. Across the full length of the trench, a decline was identified in both the co- and cross-polarization response. This observed variation in backscatter was small compared to the previous trench, but did indicate a changing interaction with the physical and/ or dielectric properties of the sub-scan target. The most evident change in snowpack composition along the trench that could have produced an attributable change in back-scatter was the increasing thickness of layer 7 and corresponding reduction of layer 6. These two mixed-layer types were composed of different grain sizes, those within the more recent layer 7 being significantly smaller in diameter. From left to right, layer 7 gradually became the dominant snowpack layer, effectively reducing the mean grain size of the snowpack. Unfortunately, the coarse range resolution of UW-Scat did not allow for characterization of individual layer contributions, and so did not offer definitive evidence of why the change had occurred.

In general, the contrasting backscatter responses of the two trench sites provided practical examples of the influence of sub-scan snow properties on Ku-band back-scatter. The findings suggest that variability in tundra snow and soil properties over short distances are significant modifiers of Ku-band backscatter and, in the future, should be considered in the development of tundra snow property retrievals. When in situ and radar measurements were averaged up to the trench (5 m) scale, there was clear sensitivity of backscatter to SWE. Comparisons at smaller scales likely require high-resolution radar systems to separate contributions to backscatter as a function of depth and horizontal location.