Tree canopy and snow depth relationships at fine scales with terrestrial laser scanning
Understanding the impact of tree structure on snow depth and extent is important in order to make predictions of snow amounts and how changes in forest cover may affect future water resources. In this work, we investigate snow depth under tree canopies and in open areas to quantify the role of tree structure in controlling snow depth, as well as the controls from wind and topography. We use fine-scale terrestrial laser scanning (TLS) data collected across Grand Mesa, Colorado, USA (winter 2016–2017), to measure the snow depth and extract horizontal and vertical tree descriptors (metrics) at six sites. We utilize these descriptors along with topographical metrics in multiple linear and decision tree regressions to investigate snow depth variations under the canopy and in open areas. Canopy, topography, and snow interaction results indicate that vegetation structural metrics (specifically foliage height diversity; FHD) along with local-scale processes like wind and topography are highly influential in snow depth variation. Our study specifies that windward slopes show greater impact on snow accumulation than vegetation metrics. In addition, the results indicate that FHD can explain up to 27 % of sub-canopy snow depth variation at sites where the effect of topography and wind is negligible. Solar radiation and elevation are the dominant controls on snow depth in open areas. Fine-scale analysis from TLS provides information on local-scale controls and provides an opportunity to be readily coupled with lidar or photogrammetry from uncrewed aerial systems (UASs) as well as airborne and spaceborne platforms to investigate larger-scale controls on snow depth.
Forests are distributed across approximately half of the snow-covered landmasses on Earth during peak snow extent (Kim et al., 2017), with snow in non-polar, cold climate zones accounting for 17 % of the total terrestrial water storage (Rutter et al., 2009; Güntner et al., 2007). Estimating the amount of water stored in this snowpack, the snow water equivalent (SWE), and its spatial distribution under various physiographic conditions is crucial to providing water managers with parameters to accurately predict runoff timing, duration, and amount, especially in a changing climate. Snowbound forested regions are rapidly changing in forest cover composition (e.g., fire, insect outbreaks, thinning) (Nolin and Daly, 2006; Bewley et al., 2010; Gauthier et al., 2015). Understanding how forest characteristics affect snow distribution, as well as how we might model the relationships between forests and snow distribution, will benefit water management objectives.
Generally, complex tree structure reduces snow deposition by increasing snow–canopy interception. However, canopy sheltering at windy sites can reverse the influence of interception on snow accumulation (Dickerson-Lange et al., 2017). Shading degrades incoming shortwave radiation, while sheltering reduces the wind speed and turbulent heat transfer within canopies, resulting in longer snowmelt duration relative to open areas. The extinction of shortwave radiation by shading, however, can enhance sub-canopy longwave irradiance from tree trunks (Pomeroy et al., 2009). Reducing wind speeds within the canopy due to sheltering can also reduce the spatial heterogeneity of snow depth and extent (Qiu et al., 2011). Therefore, at windy sites, studies have shown similar snow deposition in open areas to that under the canopy (Dickerson-Lange et al., 2017), changing sub-canopy deposition and accumulation. These and other studies demonstrate the complexity between snow processes and vegetation in the presence of other predominant controls for modeling snow distribution and properties.
Forest canopy cover can be incorporated into watershed and regional-scale models as subgrid parameterization via snow depletion curves by relating canopy cover distributions to fractional melt patterns (Dickerson-Lange et al., 2015; Homan et al., 2011; Luce et al., 1999). Pixel-level binary or weighted snow depth correction factors in gridded models (Hedrick et al., 2018; Winstral et al., 2013) can be adjusted for canopy cover, as well as a hybridized approach that adjusts radiative inputs differently in open areas and forest gaps based on their size and relationship to the surrounding forest (Seyednasrollah and Kumar, 2014). In research pertaining to forest-snow processes, forest plots may be classified qualitatively (e.g., Dickerson-Lange et al., 2015; Pomeroy et al., 2009) or more recently, at larger scales, quantitatively with airborne lidar (e.g., Mazzotti et al., 2019). The use of lidar in spatially distributed modeling efforts is rapidly advancing (e.g., Hedrick et al., 2018; Painter et al., 2016), and understanding how best to describe forest characteristics (cover, structure, gaps, etc.) relevant to snow distribution is evolving (Jenicek et al., 2018; Mazzotti et al., 2019; Yang et al., 2020).
Airborne lidar has been used to describe snow depths in forests starting almost two decades ago (e.g., Hopkinson et al., 2004) and, more recently, to describe the relationships among forest characteristics and snow distributions (e.g., Moeser et al., 2015a, b; Mazzotti et al., 2019; Zheng et al., 2016; Tennant et al., 2017). Realizing airborne lidar's ability to provide high-resolution snow depth and canopy measurements across large extents, studies have identified vegetation characteristics as drivers of snow depth variation. For example, canopy structure along with the forest canopy edge were driving factors that governed the snow depth distribution in a study of alpine climates (Mazzotti et al., 2019). Similarly, mean distance to canopy and canopy closure have been identified as strong metrics for predicting snow interception (Moeser et al., 2015a). In the wind-dominant case, Trujillo et al. (2007) observed that snow depth variability occurs at larger scales than those related to vegetation. They found that when canopy interception is dominant and wind effect is minimal, the variation in snow depth is controlled by vegetation characteristics. Broxton et al. (2015) found canopy–snow interception and shading properties in transition zones result in different snow depths in comparison to the open and under-the-canopy regions. Further work in snow depth variability near forest edges acknowledges that snow depth variations are due to the effects of temperature, wind speed and direction, solar radiation, and forest distribution (Currier and Lundquist, 2018). Recently, uncrewed aerial systems (UASs) have been utilized to measure snow depth using photogrammetric techniques (e.g., structure from motion; SfM) in open and sparsely forested areas (Bühler et al., 2016; Cimoli et al., 2017; Harder et al., 2016; Lee et al., 2021; Jacobs et al., 2021). In addition, a lidar mounted on a UAS can be collected at different scans angles, making it a reliable source for sub-canopy measurements and across catchment scales (∼5 km2) (Harder et al., 2020). UAS-based observations can fill measurement gaps in airborne and spaceborne lidar measurements and provide the opportunity to assess forest and snow relationships at a spatial (and temporal) resolution higher than airborne lidar and from a different viewing angle than terrestrial laser scanning (TLS).
Terrestrial laser scanning provides plot-level observations between forest cover and snow distribution that can be used to validate UAS, airborne (e.g., Currier et al., 2019), and spaceborne lidar and confidently upscale local-scale processes (Revuelto et al., 2016a, b). Complementary to nadir observations, TLS provides data collection with viewing angles from the ground and thus can capture fine-scale vegetation structure (and corresponding snow depth variations). Many studies have used TLS data to validate snow depths and melt (e.g., Deems et al., 2013; Hartzell et al., 2015; Grünewald et al., 2010), and along with physical modeling, to understand the role of wind in snow accumulation (e.g., Schirmer et al., 2011). While fewer studies have used TLS to explore forest canopy–snow relationships, TLS provides exciting opportunities to investigate fine-scale processes controlling snow distribution (Revuelto et al., 2015, 2016a, b; Gleason et al., 2013). Revuelto et al. (2015, 2016a) found smaller snow depth differences between the canopy and open areas in regions of thicker snowpack using TLS. They also demonstrated that shallower snow (snow depth <0.5 m) occurred closer to the trunks, while deeper snow (snow depth >0.5 m) was found at the edge of the canopy where the dominant species was Pinus sylvestris. Gleason et al. (2013) used TLS to map tree stem density in burned forests and related this to greater snow accumulation in comparison to unburned areas. Taken together, previous studies point to the importance of choosing proper scales to study the controlling processes on snow depth variability, and furthermore, the opportunities to explore relationships between snow depth and canopy structure at fine scales (individual trees).
The objective of this study is to further contribute to the understanding of fine-scale forest canopy–snow interactions by exploring how forest canopy structure affects snow depth distribution during the snow accumulation period with TLS. This study is part of the NASA-led SnowEx 2017 campaign aimed at evaluating remote sensing snow properties with a primary focus on testing the impact of forests on remote sensing approaches for monitoring SWE. We use TLS data collected during the accumulation period (single measurements) in midwinter during SnowEx 2017 (winter 2016–2017) across a number of small TLS study sites in Grand Mesa, CO. In this study, we explore the following questions:
What measures of vegetation best describe a relationship with snow depth under the canopy (sub-canopy)?
Are there conditions in which vegetation characteristics are a more important control on snow depth than topography, or vice versa?
Does snow depth vary as a function of distance from the canopy edge? How does tree height influence snow depth as a function of distance and direction?
The TLS data were collected at six sites (A, F, K, M, N, and O) across Grand Mesa, Colorado, USA. Grand Mesa is an approximate 470 km2 plateau with elevation of 2922 to 3440 m, rising along a west-to-east gradient (Fig. 1). Vegetation in the west, where wind speeds are highest, is predominantly shrubby cinquefoil (Dasiphora fruticosa) steppe with isolated Engelmann spruce (Picea engelmannii) tree islands. The central portion of the mesa becomes semi-continuous forest cover consisting primarily of Engelmann spruce with minor subalpine fir (Abies lasiocarpa) and aspen (Populus tremuloides) trees, all interspersed with subalpine meadows. Farther to the east, where wind speeds are lowest and elevation drops, there is dense continuous Engelmann spruce and subalpine fir forest with some lodgepole pine (Pinus contorta var. latifolia) and aspen stands at the lowest elevations.
Wind speed data during our TLS data collection period were available from three stations including a site at the western extent of forest cover on the plateau (Mesa West, near site A), a site termed the local-scale observation site (LSOS), and a site situated in more dense forest in the middle of Grand Mesa (Mesa Middle, near site M) (Paul Houser, personal communication, 2017) (Fig. 2). The data were collected from 17 November 2016 to 28 February 2017 and indicate a dominant NE wind direction at site A, though up to 15 m/s wind speeds from the SW were observed at this site. The predominant wind direction was from the NW at LSOS, and from the NW and SE at site M, during the sampling period. In analyses outlined below, we utilized a general E–W direction for testing the importance of wind (whereas we used a N–S direction for testing shading effects on snow; more below).
3.1 Data and processing
We collected TLS data in snow-off (fall 2016) and snow-on (winter 2017) conditions at Grand Mesa at several sites (Fig. 1, Table 1) (Glenn et al., 2019; Hiemstra and Gelvin, 2019). The winter 2017 data collection occurred over 16 d but without significant snowfall between days. Each site was scanned once during the duration. A Riegl VZ-1000 (1550 nm) and Leica Scan Station C10 (532 nm) were used. Multiple scans (at least three) were obtained at each site to reduce occlusion. The scans were coregistered to produce a single point cloud for each site and date. Coregistered scans were then georegistered using surveyed locations within the plots. The georegistered scans (i.e., area of analysis) for each site range from approximately 10 000 to 38 000 m2 (Table 1).
The TLS data were then utilized to derive snow depths, vegetation metrics, and topographic indices. From these data, we utilized multiple linear regression to investigate relationships between the canopy and snow depths under the canopy at each of our sites. Snow depth relationships with topography in open areas with no trees (of a least 0.5 m height) were investigated using decision tree regression. Methods of identifying individual trees, under the canopy and in the open areas, are described below.
The TLS point clouds were classified into ground or vegetation (fall 2016 dataset) and snow or vegetation (winter 2017 dataset) and then used to estimated snow depths at each of the sites, using several subroutines in CloudCompare (v2.11 alpha; retrieved from http://www.cloudcompare.org/, last access: 29 July 2020). The TLS data were also used for individual tree segmentation and to extract vegetation parameters using R 3.5.3 (R Core Team, 2019), lidR (v3.1.1; Roussel et al., 2020), and rLiDAR (v0.1.1; Silva et al., 2020) packages. These steps are outlined in Fig. 3.
While we did not independently assess the snow depth accuracy of the TLS data, Currier et al. (2019) assessed the relative accuracy of the same TLS data to airborne lidar at two of our sites. They indicate that the median snow depth difference between the datasets (TLS and airborne) at sites A and K was less than 5 cm.
3.1.1 Ground, snow, and vegetation classification
The CAractérisation de NUages de POints (CANUPO) method in CloudCompare was utilized to separate vegetation from ground and snow returns. This method includes training and classification. In the training step, we used 10 000 snow and vegetation samples to construct the classifier. We trained the algorithm at 15 different scales to assign features related to each class and selected the nine best combinations of scales (0.1, 0.2, 0.25, 0.5, 0.75, 1, 2, 3, 5 m) to properly separate different classes. The combination of information from these scales helped the algorithm detect the dimension of each feature and assign snow and vegetation labels to the unclassified point clouds (Lague et al., 2013). CANUPO misclassified snow data points near tree stems as vegetation, and thus we reclassified these points manually using TerraScan software (Helsinki, Finland). Manual classification included visually separating snow under the trees from tree trunks.
3.1.2 Snow depth estimation
The M3C2 algorithm (Lague et al., 2013) in CloudCompare was used to estimate under-canopy and open-area snow depths. In this algorithm, for every single point in the ground point cloud, a cylinder was defined with a range of different radii (projection scales) varying from 10 cm to 3 m and a length (height) of 3 m (see Lague et al., 2013, for details on these parameters) (Fig. B1). The orientation of the cylinder was along the normal vector of planes fitted on the ground points within a 10 cm radius. We projected all points within the cylinder onto the cylinder axis and took the vertical distance between projected snow and ground points as the snow depth estimation. Through iteration, we found a balance between including enough TLS points for subsequent analysis and the accuracy of the snow depths (assessed with standard deviation) by using a 1 m projection scale. The resulting snow depth measurement has a relative accuracy of approximately 2.5 cm based on the maximum standard deviation from M3C2. Utilizing these measurements, we compared snow depths under the canopy and in the open areas at each site. We also defined a transition zone as a 10 m buffer beyond each tree polygon in the direction of the open areas to identify any relevant differences within this zone.
3.1.3 Individual tree segmentation
We developed a canopy height model at 0.5 m resolution and identified tree tops to segment individual trees in the R package lidR. A local maximum was detected to identify tree tops using window sizes ranging from 1–3 m and minimum tree heights from 2–6 m, depending upon the site. For areas with lower tree heights (0.5–2 m), we tiled the data that contained these trees and segmented them in a similar approach. This allowed us to more accurately segment distinctly shorter and taller tree populations within sites by adjusting segmentation parameters that worked better for those areas. Based on our preliminary analyses, the Marker-controlled watershed segmentation algorithm was most accurate (compared to li2012, dalponte2016, and watershed, all available in the lidR package). In addition, in cases where tall and short trees were close to each other, the algorithm could not detect shorter trees with large crown radii. Conversely, the branches far from the top of the tree may be considered as an individual tree if a small crown radii is used. This problem was resolved by tiling the las files, processing each separately, and then combining the results. An example of the segmentation results from site F is shown in Fig. B2. A similar process was performed for all sites.
To define “under the canopy” and “in the open”, we first performed segmentation to identify individual trees. Under the canopy was defined by all snow depth points within the tree polygons. To define the open area, we merged individual tree polygons that were less than 3 m from each other (patches of trees) and used the remaining areas as open. Site A was the only site dominated by shrubs (Fig. 1, Table 1), and we considered the shrub area as open (we removed shrubs in the processing and retained the ground points below) at this site because the focus of our study was on tree–snow relationships.
3.1.4 Vegetation and topography
We computed three vegetation metrics (Fig. 4) for each individual tree identified in the segmentation process (Table A1). These were then utilized, along with topographic metrics, to predict snow depths at each site using a multiple linear regression. Trees with at least 50 % snow cover below the tree crown (based on the segmented tree polygons) were used for analysis. The metrics included foliage height diversity (FHD), crown volume, and the cumulative percentage of vegetation returns (zpcum). FHD represents the complexity of multi-layered vegetation structures (Clawges et al., 2008; Simonson et al., 2014). Trees with lower FHD have a lower number of layers and thus less interception with snow. Crown volume describes the overstory cover of individual trees and is estimated by multiplication of crown surface area by crown height. Studies have shown overstory cover is negatively related to snow depth under the canopy (Hanley and Rose, 1987). Note that high crown volume does not necessarily equate to high FHD. The cumulative percentage of vegetation returns assessed across multiple layers within a tree allows us to understand whether a tree (as a whole) or a specific layer (cumulative) of the tree crown controls snow accumulation. We used 10 layers, starting at the bottom of each tree crown. In our preliminary analyses, we used the first cumulative layer that explains the majority of vegetation returns within the crown (the first layer in which zpcumx >50 %). The zpcum4 met this threshold at site A and zpcum5 met this threshold for all other sites. By using these metrics, we are able to examine the effects of structural complexity (FHD), a specific cumulative layer (zpcumx) within the canopy, and/or the crown volume as a whole on snow depth.
Topographical metrics like elevation, eastness (sin (aspect) × slope), and northness (cos (aspect) × slope) are possible controls on snow depth for both under the canopy and in open areas. We assumed that eastness represents the effect of wind based on the predominant wind direction at the study site and northness expresses the effect of solar radiation on snow. Slope and aspect were derived for each site using a nearest-neighbor method in ArcMap 10.4.1 (ESRI, 2015) at 1 m grid resolution.
To investigate the collinearity amongst and between the vegetation and topographic metrics, a variance inflation factor was computed. The variance inflation factor was close to 1 for all metrics at all sites except site O. The metrics were standardized to make sure that the scale of the independent variables did not affect the regression. We then used the vegetation and topographic metrics for each site (except site O) in a multiple linear regression model to assess their effect on snow depth under the canopy.
At site O and in the open areas, we utilized a decision tree regression in lieu of the multiple linear regression model. In the open areas, we examined the effect of elevation, northness, and eastness on snow depths. Splits in the decision tree continued until the model could not improve beyond R2=0.001. To avoid overfitting, we validated the model by a range of complexity parameters (from 0.001 to 0.2) and pruned the tree by choosing the one with the smallest cross-validation error. We trained the tree using 70 % of the data and validated the model prediction using 30 % of the data.
3.1.5 Influence of canopy edge on snow depth
Individual trees were used to assess snow depth variation at distances of 1 to 10 m away from the canopy edge. This represents how snow depth changes from the edge of individual trees to the open areas within a 10 m distance from the edge. We subsampled our data to only include trees that had good snow coverage (from TLS) within the buffer. This was determined based on the area around the tree having at least 50 % snow cover (see above).
Snow depth variation from the edge of trees had both increasing and decreasing trends. Thus, we split the data between increasing and decreasing snow depth trends and fit a model to each. We standardized the snow depth for each 1 to 10 m interval of individual trees. This allowed us to investigate all of the changes in snow depth across the same scale. We fit logarithmic (standardized snow depth is the sum of the intercept and coefficient multiplied by the log (distance)) and linear (standardized snow depth is the sum of the intercept and coefficient multiplied by the distance) models to the increasing and decreasing snow depths, respectively, for both individual sites and all sites together.
3.1.6 Gap distribution and directional analysis
We explored whether any of our sites were suitable for understanding the role of forest gaps (i.e., shading, interception) on snow depth distributions. While our study was not designed to analyze a range of gap distributions, the inherent forest density and distribution gradient that spanned our sites across Grand Mesa provided this opportunity. In particular, we sought to identify if sites had a dispersed tree pattern, such that the gaps were large enough to prevent canopy interception of snow and thus accumulated deeper snow. Seyednasrollah and Kumar (2014) used a relationship of tree height and gap radius for evaluation of net radiation. We derived a similar but simplified gap distribution approach (Eq. 1). We calculated the average distance of 10 nearest trees to each individual tree. This gave us a rough estimate of a gap size around each tree (D). In the next step, we divided that average distance (D) by the average height (H) of those 10 nearest trees (). This ultimately provides a ratio by which we can investigate the impact of shading from trees on gaps combined with gap size.
Equation (1) illustrates the gap distribution for an individual tree (j), where Dj is the mean distance of the k closest trees to tree j; Hj is the average height of k closest trees to tree j; k is the number of neighbors; and dij and hij are the distance and height of tree i to tree j, respectively.
Secondly, we performed an average nearest-neighbor analysis of the distribution of trees at each of the sites. In this analysis, we tested for tightly clustered trees in which gaps were minimal (clustered), randomly distributed trees where gaps could potentially lead to deeper snow accumulation (random) or dispersed trees where no particular pattern exists, and thus gaps are likely not prevalent (dispersed).
We also investigated whether relationships between tree heights and snow depth variation are significant based on direction. We did this using the 10 m transition zone (buffer) for each individual tree. We classified snow depths within each buffer in the four cardinal directions and fitted a linear (snow depth = ) or non-linear (snow depth = ) model, depending upon the site, between tree heights and mean snow depth per each direction. We also performed a directional analysis with a Wilcoxon signed-rank test for comparing snow depth on the north and south sides (and east and west) for individual trees at each site. Note that due to sampling extents, our transition zone analysis was performed at 1 m increments instead of at multiples of mean tree height as in previous literature (e.g., Currier and Lundquist, 2018).
4.1 Snow depths
Using our individual tree analysis, we found higher snow depths (1–1.6 m on average) in open regions and lower snow depths in areas dominated by trees (0.8–1.3 m on average) (see Figs. 5 and 6). Snow depths were 12 %–28 % higher in the open than under canopy. Mean snow depth percent change between the 10 m transition zone and under the canopy ranges from less than 1 % for sites A and K to a maximum of 7 % at site M. We found the lowest mean snow depths in our most westerly site (A), which is dominated by dense clusters of relatively rigid shrubs (Dasiphora fruticosa) and has the lowest tree cover of all sites. The standard deviation (SD) of snow depths was similar between the transition zone and under the canopy for four sites (A, F, K, and O). We found a lower SD of open-area snow depths at site O compared with under-canopy and transition zones (Fig. 6).
4.2 Influence of vegetation and topography on snow depth under the canopy
A multiple linear regression model was applied to assess the effect of vegetation and topographical metrics on snow depth under the canopy. The regression explained 43 %, 54 %, 27 %, 25 %, and 28 % of snow depth variation at sites A, F, K, M, and N, respectively (Table 2). Based on the models, FHD was the most influential vegetation metric at five sites (Table 2). Figure B3 shows the distribution of FHD at each of the sites, with higher FHD demonstrating more evenly spaced foliar arrangement along an individual tree. Most of the sites had two peaks of FHD distributions. FHD and snow depth were negatively related at all sites, i.e., a vertically sparse foliar arrangement resulted in higher snow depths. At site A, a negative relationship (−0.21) between cumulative percentage of returns within the fourth layer (zpcum4) and snow depth occurred. FHD also showed a higher negative relationship at this site (−0.27) with snow depth. The results indicate that the effect of eastness, northness, and crown volume was not significant (p value >0.001), and elevation positively affected (with a coefficient of 0.14) the snow depth under the canopy at this site. At site F, elevation and FHD were the most important features that explained 54 % of snow depth variation. Vegetation and topography could not explain more than 30 % of snow depth variance under the canopy at sites K, M, and N.
Because of collinearity between eastness and northness at site O, we used a regression tree to investigate the effect of different features on snow depth under the trees. Eastness and FHD were the most important features at site O, respectively (Fig. 7). A decision tree regression for this site explains 74 % of snow depth variance under the trees. The results also indicate that as we move from east (positive) to west (negative), the snow increases with higher slopes. In other words, larger, west-facing slopes are covered by deeper snow. In addition, shallower snow depths are predicted in the canopy with higher FHD at this site.
4.3 Influence of slope, aspect, and elevation on snow depth in open areas
We examined the effect of topography on snow depth in open areas using a decision tree regression for each site. Based on the regression tree (Table 3), elevation was the most important feature at sites A, F, and K and was the second most important feature at sites M and N. Decision trees could predict 38 %, 36 %, 36 %, 31 %, 18 %, and 64 % of snow depth variations at sites A, F, K, M, N, and O, respectively. The model slightly overfitted for sites A, M, and N. However, the R2 values for the training and testing datasets at the other three sites are similar. Eastness and northness represent wind and solar radiation impacts on snow depth variation with regard to topography. Except site O where topography (eastness and northness) explained 64 % of snow depth variation, topographical metrics could not explain more than 38 % of snow depth at the other sites (Table 3). This is likely a result of scale, in which our plot sampling size did not adequately sample the effects of topography and wind on snow depth variation.
We found that at site A, elevation and northness were influential for snow depths in the open. High snow depths were found in open northeast-facing slopes (same as the predominant wind direction) at site A (see Figs. 1, 8b). Site O was the only site that we found an influence of both eastness and northness on snow depth. The influence of eastness occurred in both the open areas and under the canopy (Table 3, Figs. 7, 8a, b). This site has high north- and west-facing slopes (in both under canopy and the open) with relatively higher snow depths, whereas south-facing slopes have relatively lower snow depths.
4.4 Influence of canopy edge on snow depth
We found that snow depths increase with distance from the canopy edge into the open for the majority of individual trees (Figs. B4–B9). However, at some sites, we found a decreasing snow depth trend by moving farther from tree edges. For example, this occurred on the northwest side of the tree patches in the southeast portion of site O. This is the area of site O where the northwest-facing slope has likely the largest influence on snow depths. The increasing snow depth trend from the canopy edge occurs in the north where snow depths are low (less than 1 m). Site A also showed a decreasing snow depth pattern in the north/northwestern sampled region, and this is likely due to northeast winds and deeper snow depths in the northeast-facing slopes in the southern portion of the site.
Results show that a logarithmic regression can explain more than 85 % of an increasing snow depth trend at each site. Figure 9a illustrates the logarithmic regression between snow depth and distance from the edge for all sites together. The model coefficients were almost the same for individual sites as well as all sites together (Table 4). This indicates that within a 10 m distance from the edge of the trees, snow depth increases with a unique logarithmic trend.
For decreasing snow depth, a linear regression explained 72 % of snow depth variation at all sites together. However, snow depth decreases at site K followed a second-order polynomial, which covers only 4 % more variation than simple linear regression. The coefficient and p values for linear regressions are illustrated in Table 5. Figure 9b also shows the regression fit between decreasing snow depth and distance from the tree edge.
4.5 Gap distribution and directional analysis
Our results show that site N has the largest median ratio (0.74) compared to all other sites of <0.5 (Table 1). Site N is the only site with a randomly dispersed tree pattern (Table A2) and thus the most likely site to experience lower interception, possibly resulting in deeper snow.
We found a negative relationship between tree heights and snow depths based on direction at sites A, K, and O (Table A3, Fig. 10). Snow depth decreased exponentially at site A with an increase in tree height. However, this relationship was linear for sites K and O and was not significant for the other three sites. An exponential fit could explain 56 %, 61 %, 76 %, and 32 % of snow depth change in the north, west, south, and east directions at site A, respectively (Table A3, Fig. 10a). We found snow depths were different between the north and south sides of trees at sites A, K, and O but not for any other sites or directions (Table A4).
We observed several interesting relationships between vegetation canopies, topography, wind, and snow depths across our sites. As expected, snow depths were deeper in the open areas compared to under the canopy. However, describing the relationships between vegetation and snow is complicated by the structure, distribution (pattern), and type of vegetation. The relationship is further convoluted by local topography and wind speed/direction. For example, we found that slope, aspect, and wind (rather than vegetation) might control snow depths at local scales at two of the sites (A and O). This is not surprising, as site A was dominated by 0.4–0.6 m tall shrubs and wind exposed, and site O had a relatively low tree canopy cover. While site A had the lowest tree canopy cover in our dataset, we only sampled the edge of a much larger patch of trees (based on field observations). Our results indicate that local topographic interactions with wind have a major influence on snow accumulation, especially when we do not consider the much larger landscape controls. While sites A and O have slopes within the overall range of all of our sites, the combination of local slope and aspect for site O appears to be the driving factor in snow depths. In fact, site O has the highest mean snow depth (1.44 m), likely due to these local site conditions.
When our analyses were confined to under the canopy of individual trees, we generally found a significant relationship between the vertical spatial arrangement of the foliage (based on the FHD) and snow depth, but this relationship did not hold across all sites. For example, FHD and northness explained 25 % of the variance of snow depth at site M. This site has the highest mean tree heights of the study. Taken together with northness as the most important feature at this site, solar radiation likely had higher control on snow depths than on the particular foliar arrangement of the trees at this site. Overall, sites M and N had the least effect of vegetation metrics on snow depth. This may be due to the vegetation patterns at these sites (under-the-canopy slope and aspect have no effect at site N; Table 2, Fig. 8a). Site M is a relatively open area with mature Engelmann spruce and subalpine fir trees in the SW and NE areas of our site. Subalpine fir trees are generally more slender than Engelmann spruce, and thus their shape may not be as influential on accumulation of under-canopy snow depths. Site N has the highest percent cover and the smallest trees (mean tree height 10.5 m, SD of 2.62 m; Table 1). This second growth canopy is the only site dominated by lodgepole pine, which are also slender. While the mean FHD is similar to the other sites, site N is the only site with trees in a dispersed pattern in which the size of the gaps likely prevents snow interception and thus provides an opportunity for snow accumulation. In fact, site N had the second-highest mean snow depth under the canopy (1.38 m, compared with 1.44 m at site O; Figs. 6 and 8a). Testing for a dispersed tree pattern could be beneficial to future studies, especially because previous research (e.g., Sun et al., 2018) found gap size to be a control on snowmelt timing; however, our study was during the accumulation phase so we cannot draw similar conclusions at site N.
Our models show that FHD is the only control on snow depth at site K, explaining 27 % of snow variation under the canopy. The standard deviation of elevation at this site is less than that at the other sites (Table 1), likely indicating that snow depth under the canopy is not affected by topography. This indicates that in the absence of large changes in topography, snow depth under the canopy is most likely controlled by trees. In the open areas, elevation and eastness are predominant controls on snow depth. The latter is perplexing because a wind effect was not observed under the canopy (Table 2) nor along east–west sides of trees (Table A4). In the absence of other information, we conclude that the spatial arrangements of the trees may shelter the open area, causing higher snow depths with no interception. Elevation and FHD at site F explain 54 % of snow depth variation, which is the greatest among the sites. The site's large standard deviation of elevation (Table 1) explains why elevation is the most important control in both under the canopy and in open areas. The predominant wind direction is from west to east at the nearby LSOS station. However, our models indicate that wind has little influence on snow distribution, and rather solar radiation along with elevation control snow patterns in the open areas at our scale of analysis.
Our canopy edge analyses generally found that as the distance increases from the canopy edge, snow depths also increase. This finding is congruent with previous studies which used airborne lidar across larger spatial extents and lower vertical resolutions in the canopy (e.g., Moeser et al., 2015a; Mazzotti et al., 2019). We leveraged the fine-scale observations in our dataset to model snow depth increases from the canopy edge and found the trend to generally follow a logarithmic model at individual and all sites together. In contrast to our observations, Hardy and Albert (1995) indicate that snow depth changes uniformly from the tree edges towards the open. However, the patterns we observed in our TLS data are similar to those Mazzotti et al. (2019) observed from airborne lidar at Grand Mesa over the same time frame. While we observed snow depth to decrease non-linearly with distance from canopy edge at one site, a linear decrease was the norm amongst sites and was likely mediated by wind and/or topography feedbacks at sites A and O. In summary, we expect snow depth increases from the canopy edge toward the open areas, but wind and topographic controls may affect this trend.
We did not find high snow depth accumulation or variability within a transition zone similar to the findings of Broxton et al. (2015). While their study included similar tree species, wind speeds, and elevation, their spatial scale of analysis was larger with the use of airborne lidar. The relation between tree height and snow depth in cardinal directions from individual trees indicates that we expect shallower snow within the 10 m transition zone from taller trees (Fig. 10). In other words, two adjacent trees with different heights affect snow depth differently in any one direction and shorter trees generally retain deeper snow in all directions. We expected the opposite to occur, i.e., taller trees should create larger shadows and provide more shading/sheltering. As our snow-on datasets are from the accumulation season, we may not see shading effects of taller trees in the transition zone; negligible melt had occurred at the time of these surveys. If our datasets extended throughout the season (our data indicate a single measurement in time), we might expect these relationships to change.
Following previous studies that show a directional relationship with snow depths (e.g., Mazzotti et al., 2019; Currier and Lundquist, 2018), we found significantly different snow depths between the north and south sides of trees at sites A, K, and O. This may be due to the local topography and wind at sites A and O. Additionally, previous lidar-based canopy–snow interaction studies (Trujillo et al., 2007, 2009; Deems et al., 2006) relied on simple canopy models using maximum height. Our results show that in nearly all situations, structural information contained in denser lidar point clouds have more predictive capability.
A limitation of our study is that the results are site specific and cannot be generalized to all forest conditions. In addition, our data are best suited to fine-scale interactions between individual trees, or clusters of trees, and under the canopy or surrounding snow depths. Data gaps may exist from occlusion within dense canopies. We minimized the effect of occlusion by performing our analysis on individual trees. Notably, the directional analysis is not affected by occlusion, as we used tree height in the analysis and trees having at least 50 % snow cover. Occlusion with TLS can be eliminated using UAS and/or airborne lidar as their nadir/off-nadir scan positions can cover the canopies at different angles. However, mapping dense canopies and mapping snow depth under dense canopies may still be a challenge. Ultimately, TLS provides data for investigating fine-scale controls and is highly complementary to UAS and airborne lidar, which can help test larger-scale features, such as gap area across space.
Our study indicates that even with fine-scale individual tree observations from TLS, vegetation structural metrics are not enough to describe snow depth during the accumulation season. Local-scale topography and wind should also be considered. While our sites were not designed solely for intercomparison, we found notable trends in our site comparisons. The vertical arrangement of foliage (e.g., FHD) of individual trees influences under-canopy snow depths, and in some cases, quite strongly, whereas cumulative percentage of returns and crown volume were less powerful explanatory variables. Further studies should be designed to test this within and between species. For example, our sites were primarily Engelmann spruce, subalpine fir, and lodgepole pine, all of which have different canopy structural shapes. Further studies targeting samples of each of these with different foliar arrangements and heights should be undertaken to fully understand the implications of FHD and tree heights on snow depths at local scales.
We also found that topography had greater control than vegetation at sites where slopes favored wind conditions for increasing snow depths, or where vegetation presence was minimal. While the latter may be obvious, increased observations with varying vegetation cover, wind, and topography should be considered with TLS.
This study highlights the complementary nature of TLS observations to UAS and airborne lidar, where TLS can provide fine-scale observations within the canopy and relationships with under-the-canopy snow depth. Data from TLS can also be used to validate airborne lidar (e.g., Currier et al., 2019), and further studies should investigate how vegetation metrics such as FHD compare between TLS, UAS, and airborne lidar in these snow-dominated forest ecosystems. Further, along with UAS and airborne lidar, TLS provides a complementary dataset for upscaling to similar types of vegetation structure and topography observed from satellites such as the NASA Ice, Cloud and land Elevation Satellite (ICESat-2) or missions such as Global Ecosystem Dynamics Investigation (GEDI).
The codes used for analysis are cited in the paper. Additional requests can be made to Ahmad Hojatimalekshah (email@example.com).
ZU, LS, CAH, CJT, AG, and NFG contributed to field data collection. LS, NFG, CAH, HPM, and AG designed the project. In addition, ZU, NFG, AH, CAH, CJT, JDG, HPM, JPM, and JE contributed to writing and interpretations. AH did the analysis.
The authors declare that they have no conflict of interest.
Support for the project was provided by the NASA SnowEx 2017 campaign and the Department of Geosciences, Boise State University. We would like to thank all those who participated and supported the NASA 2017 SnowEx campaign.
This research has been supported by NASA (grant nos. 80NSSC18K0955 and NNX17AL61G).
This paper was edited by Chris Derksen and reviewed by Phillip Harder and one anonymous referee.
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