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 The timing and amount of snowmelt from forested watersheds is influenced by the total radiation reaching the forest floor. In order to understand and predict the impact of natural or anthropogenic changes in vegetation density on snow energetics, it is important to first quantify the relationship between vegetation density and net snow cover radiation. A physically based forest radiation model (FoRM) was developed to quantify net radiation on the forest floor and its dependence on vegetation density in midlatitude coniferous forests. For clear sky conditions, net radiation on the horizontal forest floor frequently exhibits a nonmonotonic decreasing then increasing trend with increasing vegetation density. The relationship turns monotonically increasing when cloudiness is considered. Variations in slope and aspect were also found to influence the behavior of radiation in relation to changing vegetation density. Net radiation increases with increasing slope for southerly aspects and decreases with northerly facing aspects. For clear sky conditions on south facing slopes, the optimal vegetation density at which radiation is minimized increases both with slope and toward more southerly aspects. In contrast, on north facing slopes, the vegetation density where net radiation is minimized decreases with increasing slope angle. When sky cloudiness is considered, for increasing south facing slopes, the relationship becomes relatively complex with the appearance of a local minimum at intermediate vegetation densities. The results have implications for prediction of snowmelt dynamics in complex terrain and development of forest thinning strategies to modulate snowmelt timing in mountainous environments.
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 Snow cover ablation is an important process that affects hydrologic states and fluxes and water resources including groundwater recharge, stream-aquifer interactions, water quality, urban and agricultural water supply, and hydropower generation [Lundquist and Flint, 2006; Stewart et al., 2005]. Decrease in snowpack amount and alteration of melt timing may disrupt agricultural and municipal water supplies [Rango and Vankatwijk, 1990; Varhola et al., 2010; Winkler and Roach, 2005]. Alteration of canopy cover may either increase or decrease the timing and rate of snowmelt depending on slope and aspect [Ellis et al., 2011], and seasonal climate conditions (J. D. Lundquist, S. E. Dickerson-Lange, J. A. Lutz, and N. C. Cristea, Temperature-induced tipping point in net effect of forests on snowmelt, Water Resour. Res., in review, 2013). One of the primary factors that influence snow energetics is the net snow cover (as an emitter and reflector) radiation [Aguado, 1985; Bohren and Thorud, 1973; Elder et al., 1991], which typically is the dominant energy flux component when turbulent fluxes are relatively small, even in forests [Link and Marks, 1999]. Prediction of snowmelt in forested settings therefore necessitates understanding and prediction of the spatial and temporal distribution of net radiation on the forest floor [Varhola et al., 2010].
 Net snow cover radiation on the forest floor (NSRF) depends on a wide range of environmental and physical parameters including solar angles (controlled by latitude and time), vegetation density and geometry, physical properties of snow and canopy such as albedo and longwave emissivity, air temperature, humidity, sky cover, and local slope and aspect [Flerchinger et al., 2009; Gelfan et al., 2004; Kaminsky and Dubayah, 1997; Kumar et al., 1997; Marthews et al., 2012; Pomeroy et al., 2009]. NSRF consists of multiple radiation components which can be broadly classified into two spectral bands: longwave (3.5–100 µm ) radiation from trees, sky and snow, and shortwave (0.28–3.5 µm) radiation that includes direct beam and diffuse radiation, and reflected shortwave from snow on the ground [Link and Marks, 1999; Pomeroy and Dion, 1996; Pomeroy et al., 2009] and canopy [Bohren and Thorud, 1973]. Several studies have evaluated individual radiation components and explored the influence of different environmental and physical variables. Longwave radiation is predominantly controlled by temperature and emissivity of the source [Awanou, 1998]. Net longwave radiation on the forest floor is influenced by the contribution of radiation from multiple sources including canopy [Gay, 1968; Gay et al., 1971; Pomeroy et al., 2009], sky [Pluss and Ohmura, 1997], and emitted longwave radiation from the snowpack [Male and Granger, 1981]. The above-canopy incoming shortwave radiation varies with solar zenith angle which depends on latitude, season, time of day, and atmospheric turbidity [Male and Granger, 1981]. In forested settings, the above-canopy radiation declines as it passes through the canopy depending on the size and location of canopy gaps, canopy leaf area [Hardy et al., 2004], leaf orientation [Monteith and Unsworth, 2008], foliage density in the crown [Hutchison and Matt, 1977], and tree geometry including height, shape, and crown base height [Davis et al., 1997; Rasmus et al., 2011]. The shortwave radiation reaching the forest floor is also modulated by topographic factors such as elevation, slope, aspect, and adjacent terrain shading [Dubayah and Rich, 1995; Ellis et al., 2011; Gustafson et al., 2010; Hendrick et al., 1971; Jost et al., 2007; Kumar et al., 1997]. Net shortwave radiation is also influenced by snow albedo which determines the amount of reflected shortwave radiation [Link and Marks, 1999].
 Evaluation of net radiation for a range of vegetation densities (from sparse to very dense forests) is challenging. Most of the efforts related to quantification of NSRF in relation to discontinuous vegetation cover have focused on conditions in isolated canopy gaps [Berry and Rothwell, 1992; Gary, 1974; Golding and Swanson, 1978; Lawler and Link, 2011] or on comparison of radiation between open and relatively homogeneous stands with a limited range of tree densities [Hardy et al., 1997; Musselman et al., 2008; Price and Dunne, 1976; Sicart et al., 2004]. Only a limited number of efforts have evaluated how variations in vegetation density influence net snow cover radiation under forest canopies [Bohren and Thorud, 1973; USACE, 1956]. An analytical model used to explore how the variation in net radiation changes with respect to vegetation density in conifer forests showed existence of a maximum net radiation for high snow albedos. For other snow albedo ranges, the relationship was found to be either monotonically increasing or decreasing [Bohren and Thorud, 1973]. In contrast, a study in a lodgepole pine forest at ~39°N latitude reported that incoming net radiation in forested areas had a minimum value at an intermediate vegetation density [USACE, 1956]. While the aforementioned research highlights the disparate relationships between snow-covered forest floor radiation to vegetation density, the controls on these relationships in relation to spatial and temporal variations of different radiation components in forested settings have not been fully quantified. Furthermore, influences of topographic characteristics such as slope and aspect on the radiation trends spanning a range of forest densities have not been evaluated.
 The primary goal of this research is to quantify and understand the controls on net radiation in relation to vegetation density for different slopes and aspects. To understand the relative contribution of different radiation components reaching the forest floor, here we present a physically based forest radiation model (FoRM) that uses discrete representations of individual trees. In this study, the model is used to predict spatially distributed radiation components in a gridded infinite forest; however, the model formulation is also generic enough to be applied for NSRF calculation within heterogeneous forest patches. FoRM can be run at relatively fine temporal scales (e.g., <1 h) and can therefore be used to assess the temporal variability of all radiative energy components ranging from daily to seasonal scales and across a range of spatial scales ranging from the tree (e.g., <1 m) to the stand (e.g., >10 m) level. Specifically, four questions using FoRM are addressed in this work: (a) How does vegetation density influence net radiation on the forest floor during clear sky conditions? (b) How does sky cloudiness alter the variation of net radiation for different vegetation densities? (c) How does slope affect the amount of net radiation for a range of vegetation densities in relation to horizontal sites? and (d) How does aspect affect the amount of radiation for a range of vegetation densities?
2 FoRM: A Forest Radiation Model
 Numerical experiments were designed to understand the variation of radiation below a coniferous forest canopy for both flat and inclined topography. The analysis was performed using virtual trees with cylindrical shaped crowns that are typical of white spruce (Picea glauca) [Gilman and Watson, 1994]. The species represents a relatively common conifer tree that is widely distributed in Northern Hemisphere forests that extend from 43° (Maine) to 69° north latitude (Alaska) [MFC, 1908; plantmaps.com, 2012] and hence was selected as a generic conifer for these investigations. FoRM accounts for modification of radiation at the forest floor due to a number of tree morphometric characteristics including height, shape, crown diameter and density, and crown base height. For simplicity, the forest was assumed to have a homogeneous gridded tree distribution, with distance between trees being equal to d. To evaluate the variation of NSRF for changing vegetation density, d was varied between experiments. Because of the symmetric arrangement and infiniteness of the forest, NSRF in each rectangular (d × d) control volume, with a tree at its center (Figure 1), is the same as the average NSRF for the whole forest.
 Net radiation on the forest floor (RNet in W m−2) is modeled as a sum of net longwave (LNet in W m−2) and shortwave (SNet in W m−2) radiation components within the control volume [Hardy et al., 1997; Pomeroy et al., 2009; Sicart et al., 2006]:
 Net radiation is positive if the radiant flux is toward the snow cover. The spatiotemporal average of net radiation, 〈NSRF〉 (W m−2), on the forest floor is calculated using
where d is distance between trees. The radiation calculation is performed between winter (t1) and summer (t2) solstices in each control volume. The simulation period spans the entire duration of the snow season for many coniferous forests in mountain environments. It is assumed that snow exists on the forest floor for the entire snow season. Notably, the analyses can be performed for any place- and year-specific snow cover duration.
 Net snow cover longwave radiation expands to
where ↓ Lcrown is incoming longwave radiation from tree crowns (W m−2), ↓ Ltrunk is incoming longwave radiation from tree trunks (W m−2), ↓ Lsky is incoming longwave radiation from sky (W m−2), and ↑ Lsnow is outgoing longwave radiation from snow (W m−2). The four longwave radiation components (see equation (3)) are computed using the Stefan-Boltzmann equation. The canopy, trunk, and sky longwave irradiances are estimated from the temperatures and emissivities of respective sources using equations (4), (5), and (6) [Essery et al., 2008a; Gryning et al., 2001; Male and Granger, 1981; Marks and Dozier, 1979; Pluss and Ohmura, 1997; Pomeroy et al., 2009; Sicart et al., 2006; Todhunter et al., 1992].
where SVF is the sky view factor, TVF is the trunk view factor, σ is Stefan-Boltzmann constant (σ = 5.67 × 10− 8 W m− 2K− 4), εsky is sky emissivity, Tair is air temperature (K), εcan is the canopy emissivity for both crown and trunk, Tcrown is crown temperature (K), and Ttrunk is trunk temperature (K). Generally, air temperature is a good estimate of crown temperature in low-insolation conditions and under relatively dense canopies during high insolation [Pomeroy et al., 2009]. However, needle and branch temperatures can exceed air temperature by about 1–2 K in low-density canopies during high-insolation conditions. Trunk temperatures can be even larger, with magnitudes as high as 20 K higher than air temperature during high-insolation conditions and around 10 K higher during low-insolation conditions [Pomeroy et al., 2009]. In the absence of any supporting data at intermediate densities, the observed temperature differences for discontinuous and dense forests from Pomeroy et al.  are used for calculation of differences between air and crown/trunk temperatures at intermediate vegetation densities (Table 1). Since shortwave radiation is a dominant control in determining how warm canopies and trunks are in relation to air temperature, observed temperature differences at Fraser Experimental Forest near Fraser, Colorado, U.S. (39.9°N, 105.9°W) [Pomeroy et al., 2009] for the two defined vegetation density extremes were regressed against modeled shortwave radiation at intermediate vegetation densities to obtain the variation of crown/trunk temperature differences with vegetation density. Additionally, sky and snow temperatures are assumed to be uniformly distributed across the control volume. Outgoing longwave radiation from snow on the forest floor to the atmosphere and tree is calculated based on [Gryning et al., 2001; Todhunter et al., 1992]
where εsnow is snow emissivity (dimensionless) and Tsnow is snow temperature (K). Snow surface emissivity is considered to be equal to 1.0 [Male and Granger, 1981], while no reflection of the longwave components from the snow surface is considered. In the analysis, snow temperature is set to dew point temperature (Tdp) when Tdp < 0°C and to zero otherwise.
Table 1. Input Parameters Used in the Model
Snow albedo for diffuse radiation (αdif)
Snow albedo for direct radiation (αdir)
Snow free canopy albedo (αc)
Snow emissivity (εsnow)
Canopy emissivity (εcan)
Crown and air temperature difference in dense forests (Tcrown − Tair)
Crown and air temperature difference in sparse forests (Tcrown − Tair)
Trunk and air temperature difference in dense forests (Ttrunk − Tair)
Trunk and air temperature difference in sparse forests (Ttrunk − Tair)
 The incoming shortwave flux incident at the snow surface consists of two components, a direct beam, ↓ Sdir (W m−2), and a diffuse component, ↓ Sdif (W m−2), while ↑ Ssnow is outgoing shortwave radiation from snow (W m−2). As the direct beam passes through the atmosphere and canopy, it is attenuated by both absorption and scattering processes. Direct shortwave radiation on the forest floor is evaluated using a probabilistic approach [Nilson, 1971] and is calculated based on [Essery et al., 2008b]
where P is the probability of a light beam not intersecting a canopy element; Sdir,open is direct shortwave radiation for open sky (W m−2) which depends on time and site latitude, slope, and aspect [Kalogirou, 2009; Kumar et al., 1997]; θ is the solar incidence angle (the angle between the Sun and normal to the surface); G is the projection coefficient of leaf orientation (dimensionless); λ is the effective foliage area volume density (m−1); and Lpath is the length of the solar beam passing through the canopy (m). Assuming a random orientation of leaves, G is assumed to equal to 0.5 in this analysis. Open sky solar radiation at the land surface varies with solar zenith angle and changes in solar distance during a year and is influenced by latitude, slope, and aspect. Open sky direct solar radiation is calculated using [Kreith and Kreider, 2011]
where Sextr is extraterrestrial solar radiation and τb is the atmospheric transmittance for beam radiation. For clear sky conditions, atmospheric transmittance is calculated using [Hottel, 1976]
where ψ is solar zenith angle; a0, a1, and k are constant coefficients; and A is the altitude of the site in kilometers. Extraterrestrial solar radiation and its variation with location and time is evaluated based on Kalogirou  and is presented in Appendix A. Diffuse shortwave radiation due to scattering is calculated based on [Essery et al., 2008b; Kumar et al., 1997]
where β is the slope and τd is the atmospheric diffusion factor. Considering that τd is a linear function of τb [Wong and Chow, 2001], a regression equation was derived from available data of clear sky days at the closest National Renewable Energy Laboratory site [NREL, 2012] in Maine (Table 2), to estimate τd in clear sky conditions:
Table 2. Location and Characteristics of the Sites Used in the Model
NCDC site at Greenville, ME (1977–2012)
Air temperature and relative humidity
Elevation: 423 m
Annual mean temperature: 4.9°C
Annual temperature range: 28.3°C
Diurnal temperature range: 9.2°C
NREL site at Millinocket, ME (1990–2010)
Solar radiation and sky cover
Elevation: 124 m
Annual mean sky cover: 56.1 %
LSOS site at Fraser, CO
Validation of shortwave and longwave radiation data
Elevation: 2780 m
 For cloudy sky conditions, τd and τb are directly extracted from NREL data by comparing diffuse and direct beam radiation with extraterrestrial radiation. Snow on the forest floor reflects a fraction of incoming direct and diffuse shortwave radiation and is calculated using [Hardy et al., 1997; Hardy et al., 2004; Todhunter et al., 1992]
where αdif and αdir are snow albedo (dimensionless) for diffuse and direct radiation, respectively. Taking into account the infinitely many reflections of shortwave radiation between the snow-covered forest floor and canopy [Bohren and Thorud, 1973], net shortwave radiation (SNet) is calculated as
where αc is canopy albedo. Notably, two variables that change with vegetation density and have a large effect on NSRF are sky view factor (SVF) and path length (Lpath). Sky view factor affects longwave radiation from the tree crowns, trunks, and sky, and diffuse shortwave radiation from the sky. Assuming that canopy structure is invariant throughout the year, SVF is only a function of location within a stand. Path length influences direct shortwave radiation. Since path length changes with the solar zenith angle and azimuth, ↓ Sdir and SNet vary both spatially and temporally.
2.1 Path Length
 The spatiotemporal distribution of path length is calculated using a ray-tracing method similar to the one discussed in Essery et al. [2008b] where path length calculations were performed for ellipsoidal crown shapes at a level site. Here, the formulation is extended to account for inclined topography and cylindrical tree shapes to represent a generic, yet physically reasonable, coniferous tree form. Path length, Lpath, is obtained by calculating the absolute difference between two positive solutions of the parametric equation representing a cylindrical crown (Figure 2a). The parametric equation for the cylindrical crown form is represented by
where (xt, yt) is the coordinate of the stem, h is tree height, hb is crown base height, and rc is crown radius. A quadratic equation for l is obtained by replacing x, y, and z in equation (19) with
where Z and Zs are the solar and surface azimuth angles, respectively. Equation (19) reduces to
where a, b, and c are
 The discriminant of equation (23) is defined as
 The path length for a single tree, Lpath,1, is the difference between two solutions of the quadratic equation and is calculated as
 In a forested setting, path lengths have to be calculated to account for the passage of beam radiation through multiple crowns. Total path length (Figure 2b) is calculated at any location by adding path lengths through multiple crowns using
where (Z − Zs) is the angle between the Sun and surface azimuths, and D is the distance shown in Figure 2b. To calculate path length through tree trunks (Lpath,1,trunk), rc, hb, and h are replaced by rt, 0, and hb, respectively, through equations (19) to (28). Because of the nontransmissive trunks, if Lpath,1,trunk > 0, P in equation (9) equals 0.
2.2 Sky View Factor
 The sky view factor (SVF) is the fraction of hemispherical sky that is viewable from a given point [Matzarakis and Matuschek, 2011]. A three-dimensional approach is used to estimate sky view factor for every grid cell on the forest floor. The hemispherical sky is meshed, and each discretized element is identified in polar coordinates (angular altitude and azimuth). The hemisphere is divided into 180 intervals along the altitude direction and 360 intervals along the azimuthal direction. On the hemisphere, a cell is marked blocked if a tree lies in the line of sight to it. Area blocked by the vegetation canopy in a certain direction (ϕ) is identified as the subtended region between tree zenith (ω) and ground along-altitude axis and between ϕ − dϕ and ϕ + dϕ along the azimuth. Tree zenith angle (ω) and central azimuth (ϕ) are calculated by
where P is the location at which SVF is to be calculated, point T is the tree base, and point I is the top of the tree. Width of the area blocked by the canopy is 2dϕ, where dϕ is
 The sky view factor calculation also accounts for incoming radiation transmitted through the canopy. A probabilistic ray-tracing method is used to estimate the sky view factor. The probability of seeing the sky, p(ω,ϕ), for open sky pixels is 1 and for blocked pixels is e− G λ L(ω,ϕ). SVF is obtained by
where γ is directional horizon angle and obtained using
 Similar to SVF, trunk view factor (TVF) is calculated when only tree trunk is considered. We call this algorithm to estimate sky view factor the SkyMap method.
2.3 Model Application
 Representative values of physical parameters including εsnow, εcan, αdir, αdif, and αc were used to calculate individual energy components of NSRF. Typical values of snow albedo and emissivity of canopy, sky, and snow are listed in Table 1. Snow albedo has a spectral variation from 0 to 0.9 depending on snow age, grain size, and wavelength [Warren and Wiscombe, 1980; Wiscombe and Warren, 1980]. An intermediate value of 0.4, representative of the seasonal average albedo in forested settings where debris deposition from the forest canopy is common [Melloh et al., 2002], was used in this analysis. Snow albedo for diffuse radiation, αdif, was set equal to 0.8 [Wang and Zeng, 2010]. Canopy albedo was set to 0.2 [Bohren and Thorud, 1973; Eck and Deering, 1990, 1992]. The emissivity of snow and canopy were set to 1.0 [Dozier and Warren, 1982; Sicart et al., 2006; Warren, 1982] and 0.98 [Pomeroy et al., 2009] respectively. Although these values for albedo and emissivity would likely differ for a given site at any given time in the snow season, they were selected as reasonable values in order to assess the relative sensitivity of snow cover net radiation to vegetation density. Clear sky emissivity depends on air temperature, pressure, and humidity [Marthews et al., 2012]. Daily clear sky emissivity (εsky,clear) is estimated using [Prata, 1996]
where w is precipitable water in the air (cm) and calculated as , e0 is ambient vapor pressure (kPa), and Tair is screen-level air temperature (K). Cloudy sky emissivity (εsky,cloudy) is obtained using Prata-Keding model, which was noted to perform particularly well for North American locations [Flerchinger et al., 2009]:
where C is the fraction of cloud cover.
 The variation of NSRF in relation to vegetation density was calculated for a white spruce forest stand near Greenville, ME (45.5°N). White spruce is a common tree species at midlatitudes to high latitudes in North America. This species is widely distributed in the boreal forest of North America ranging from mountainous areas in the west to coastal regions in the east. White spruce has a cylindrical crown shape and can grow up to 28 m in height and 6 m in width [Arbor Day Foundation, 2012; MFC, 1908]. This species and location were selected as a generic representation of midlatitude North American sites where there is considerable interest in understanding the effects of coniferous forest densities on seasonal snow energetics. In this analysis, we consider a typical tree dimension, with crown radius, rc, being equal to 3 m; tree height, h, being equal to 24 m; and tree trunk radius, rt, being equal to 0.4 m. The model was run using a meteorological data set such as air temperature and relative humidly from National Climatic Data Center (NCDC) meteorological station near Greenville, ME [NCDC, 2012] and cloud cover data obtained from NREL [NREL, 2012]. The site has long-term air temperature (1977–2012) and solar radiation (1990–2010) data. Relevant information about the site is listed in Table 2. Given the absence of effective foliage area volume density (λ, equation (9)) information for white spruce, λ was estimated based on allometric relationships for Engelmann spruce, which has a similar structure [Kaufmann et al., 1982]:
where dc is crown vertical depth and was assumed to be equal to 20 m. In this paper, the vegetation density is presented as , where d is the distance between trees. Canopy closure (cc), an alternate metric, used in the literature [Reifsnyder and Lull, 1965] to quantify vegetation density, can be related to d as .
 All the radiation components (equation (1)) were calculated on a 200 × 200 grid within a control volume (Figure 1b) for vegetation densities of ranging from 0.005 m−1 to 0.17 m−1, where d is distance between trees. The average net radiation from 21 December to 20 June, calculated on 40,000 grid cells, was then used to evaluate the variation of net radiation in relation to vegetation density (). Comparison of Sdir and Sdif from the model (equations (10) to (16)) for open clear sky conditions against NREL data, at the site closest to Greenville, ME, showed an adequate match (Figure 3, R2 = 0.91 for direct radiation and R2 = 0.45 for diffuse radiation). Incoming shortwave radiations obtained from FoRM were compared against observed data, both above and underneath the canopy, in a uniform lodgepole pine forest at the Local Scale Observation Site (LSOS, [NSIDC, 2013]) in Fraser, CO, U.S. (39.9°N, 105.9°W, elevation = 2780 m). Measured incoming longwave radiations at the LSOS, both above the canopy and on the forest floor, were also compared with the radiation derived from the model. Details of the shortwave and longwave radiation observation experiments can be referred in Hardy et al.  and Pomeroy et al. , respectively. The model was run for representative tree geometry (h = 12.6 m, dc = 8.8 m, rc = 1.38 m, rt = 0.18 m) and canopy closure (cc = 47%, d = 0.28 m−1) at the site. Although shortwave radiation shows a strong spatial gradient at the site, the modeled shortwave radiation reasonably reproduces both the temporal trend (R2 = 0.80) and integrated mean observed data (1.5% difference in the total energy received at the forest floor, Figure 4a). The comparisons of longwave radiations between the model and the observations also show satisfactory correlations (R2 = 0.81 for above the canopy and R2 = 0.93 for the forest floor). Moreover, the difference of total longwave radiations as estimated by the model and the observations are minuscule (0.6% for above the canopy and 1.2% at the forest floor, Figure 4b). Due to logistical challenges associated with the measurement of distributed radiation across a range of vegetation densities, especially for different slopes and aspects, net shortwave radiation for a range of vegetation densities remain unvalidated. It is to be noted that the equations used to calculate the individual radiation components in FoRM have been previously validated in the referenced literature and given the acceptable validation at control sites; this model is considered to be reasonable to advance insight into the controls of vegetation density on net snow cover radiation.
3 Results and Discussion
 The results are presented thematically, following the questions outlined previously.
3.1 Vegetation Density Influence on Net Radiation at the Forest Floor for Clear Sky Conditions
 The spatiotemporal variation in ↓ Sdir is primarily due to variation in Sdir,open and shading fractions. Figure 5 shows the temporal variation in Sdir at two orthogonal points on the forest floor (P1, P2) that are located at a distance of and , respectively, from a tree in the spatial domain shown in Figure 6. The two points provide information about the spatiotemporal variation in radiation for a relatively sparse forest at locations that are at distinct distances and directions from an individual tree. ↓ Sdir at these two points is equal to Sdir,open, unless they are shaded. The magnitude of ↓ Sdir in shaded regions is dependent on path length (Lpath), which changes with Sun angle and tree spacing. As the number of trees along the direct beam path increases, Lpath also increases, and hence ↓ Sdir is less due to absorption and scattering by the canopy. For example, P1 is shaded around noon, by both the center tree and the tree directly south of it (see Figure 6). As a result, over time, the path length first increases due to the solar beam passing through one tree crown and then through two tree crowns, resulting in a dome-shaped variation in Lpath that peaks at solar noon (Figure 5a). For the same period, ↓ Sdir at P2 is markedly different. Notably, during early and late hours of the day when the Sun is closer to the horizon, Lpath increases to a very high value at both P1 and P2 (Figures 5a and 5b). Both increase in ↓ Sdir and decrease in shading fraction contribute to an increasing trend in net shortwave radiation with decreasing solar zenith angle on a flat forest floor. The phenomenon is evident in Figure 6 where in the morning of 21 December (9:00 A.M. local standard time), shadows are relatively long and oriented in the northwest direction. At this time, 69% of the control volume basal area is shaded, and the ratio of average shortwave radiation in the forest to an open area, or forest transmissivity (τ), is about 37%. At noon, tree shadows are smaller, hence the shading fraction is only 25% of the control volume area, and τ = 76%. In the afternoon (2:00 P.M. local standard time), tree shadows start increasing again and shading fraction increases to 62% of the control volume area. In this case, τ reduces to 46%. For the same time of the day in spring, shading fraction is lesser and forest transmissivity is greater, relative to the winter, due to higher Sun angles (Figure 6).
 Irrespective of the timing, shading fraction on the forest floor increases with increasing vegetation density (larger ), hence ↓ Sdir decays monotonically with increasing (Figure 7a). Increase in also leads to a decrease in sky view factor. Therefore, ↓ Sdif also decreases in high-density forests (equation (14)). The outgoing shortwave radiation component, ↑ Ssnow, also decreases with increasing , as it is proportional to the summation of ↓ Sdif and ↓ Sdir (equation (17)). As both incoming shortwave components and the proportional outgoing component exhibit a monotonic decreasing trend with vegetation density, SNet decreases with increasing as expected (Figure 7b).
 The three longwave components vary differently in relation to vegetation density. ↓ Lsky varies inversely with . This is because ↓ Lsky is directly proportional to the sky view factor that decreases with a denser tree spacing. On the other hand, ↓ Lcrown and ↓ Ltrunk increase in denser forests. Because of the higher emissivity of the canopy and trunk relative to the sky, longwave radiation from trees (↓ Ltree = ↓ Lcrown + ↓ Ltrunk) in very dense forests (SVF → 0) is greater than ↓ Lsky in the open area (SVF = 1), and LNet (see equation (3)) therefore increases with , as expected (Figure 7b).
 The increasing LNet and decreasing SNet trends with leads to an interesting variation in NSRF. Due to a small shading fraction at very low vegetation densities ( < 0.02 m−1 or cc < 2%), the rate of decrease in SNet is relatively less than the rate of increase in LNet. Therefore, the maximum NSRF occurs for very sparse forests ( ≈ 0.02 m−1 or cc ≈ 2%) and is around 5% more than in open areas; however, for forests with density > 0.02 m−1 (cc > 2%), NSRF exhibits a different trend with changing vegetation density. In sparser forests (lower ) where SNet is relatively large and LNet is negative, NSRF decreases in relation to . In denser forests (higher ), SNet is negligible and NSRF increases with increase in LNet as vegetation density further increases. As a result, NSRF is minimum for intermediate forest densities ( ≈ 0.12 m−1 or cc ≈ 40%) for clear sky conditions. At the minima, NSRF is about 74% less than the open areas and 23% less than very dense forests ( > 0.16 m−1 or cc > 75%). Occurrence of a minimum in intermediately dense forests with about 40% canopy closure ( ≈ 0.12 m−1) is similar to results derived from an empirical model in lodgepole pine forests in California ~39°N [USACE, 1956] and the reported results for a coniferous forest in Oregon ~44°N [Reifsnyder and Lull, 1965].
 The noted trends of net radiation and magnitude of optimal vegetation densities that minimize NSRF obtained here are dependent on the time period of analysis and the representative values of parameters (e.g., snow albedo) used in the radiation calculations. Notably, since both ↓ Lsky and ↓ Ltree (= ↓ Lcrown + ↓ Ltrunk) vary with the fourth power of Tair, the relative contribution of LNet and SNet is dependent on Tair. As a result, the variation of both NSRF with and the density at which NSRF is minimized, is also dependent on Tair. Considering all other parameters to be the same, increase in average air temperature for the site will increase LNet. Increase in LNet due to temperature effects is higher in dense forests than sparse forests (because of εsky < εcan), resulting in the occurrence of the NSRF minima at lower vegetation densities (Figure 8a). The results are also affected by the assumption of clear sky conditions during the entire snow season. Although the majority of the radiation during the analysis period is received during late spring and early summer which are generally characterized by clear days, a large number of cloudy days will increase the sky emissivity and LNet and decrease incoming shortwave radiation and SNet. In this scenario, the minimum NSRF may occur at a very low vegetation densities followed by a monotonic increasing trend with vegetation density which is discussed in section 3.2. Differences may also be expected for different canopy and trunk temperatures. For warmer canopy and trunk temperatures, with temperature difference to air temperature being twice of what was considered in the base simulation, the increase in LNet is larger in very dense forests (ΔLNet ≈ +6 W m−2) rather than very sparse forests (ΔLNet ≈ +0.5 W m−2), resulting in a marginal decrease in the optimal density where radiation to snow is minimized. For colder canopy and trunk (Tcan = Tair) conditions, LNet changes with the similar trend but in the opposite direction (ΔLNet ≈ −6 W m−2 in very dense forests and ΔLNet ≈ −0.5 W m−2 in very sparse forests), leading to a higher optimal density. Due to gradual changes in ΔLNet from low to high densities, changes in the optimal density with Tcan are negligible (Figure 8b). Differences in snow temperature (δTsnow) affects NSRF by uniformly increasing or decreasing the LNet (≈ 4σεsnowTsnow3δTsnow) for all vegetation densities, while SNet remains unchanged. This will lead to a uniform change in NSRF and hence no change in the optimal density (Figure 8c). We also note that an average snow albedo of 0.4 was used for the duration of analysis. Accounting for temporal variations in albedo over the entire snow season resulting from variations due to snow aging and angular effects will influence the outgoing shortwave radiation and hence the variation of NSRF with . Higher albedos reduce SNet, leading to decrease in NSRF and the optimal density (Figure 8d). Similarly, SNet is reduced by clumping (e.g., conifers; low Gs) and in species with relatively scattered canopy structure (low λs), leading to decrease in NSRF and the optimal density (the data are not shown). Despite these assumptions, this research clearly indicates that a net radiation minimum can occur in forests with intermediate densities and that physically based radiation transfer modeling based on discrete trees can be used to assess how the minimum point varies as a function of key variables that control snow cover energetics. Future work geared toward refining and accounting for snowmelt timing changes with will consider coupled changes in albedo, radiation, and snow cover dynamics.
3.2 Vegetation Density Influence on Net Radiation at the Forest Floor for Interspersed Clear and Cloudy Sky Conditions
 To consider effects of sky cloudiness on NSRF, the model was run using daily cloud cover data obtained from the closest National Renewable Energy Laboratory station to the studied site in Maine. Daily averaged τd and τb were also derived from NREL data set to estimate direct and diffuse shortwave components for cloudy sky conditions. Corrected sky emissivity was calculated using equation (36). Results suggest that compared to clear sky conditions, all incoming radiation components are affected by interspersed cloud cover. Cloud cover leads to higher sky emissivity resulting in an increase in ↓ Lsky, while lower insolation may cause a decrease in canopy temperature contributing to a minor decrease in ↓ Lcrown and ↓ Ltrunk [Pomeroy et al., 2009]. As a result, increase in LNet in open areas was ~15% larger compared to clear sky conditions. Effect on LNet is negligible in very dense forests ( >0.16 m−1) (Figures 7b and 7d). Shortwave radiation components are also influenced by cloud cover. Cloud cover reduces the direct shortwave component by increasing atmospheric extinction and enhances the diffuse shortwave component by increasing atmospheric scattering. As a result, global incoming shortwave radiation (↓ Sdir + ↓ Sdif) decreases by ~52% compared to clear sky conditions (Figures 7b and 7d). Since the rate of decrease in shortwave radiation is markedly larger than rate of increase in longwave radiation, NSRF shows a monotonic increasing behavior with increasing vegetation density (Figure 7d). For locations with higher average of cloud cover than the studied site (the average cloud cover for Greenville, ME is about 56%), NSRF is expected to expose a relatively rapid increase with vegetation density rather than the obtained results.
3.3 Effect of Slope on the Variation of Net Radiation in Relation to Tree Spacing
 To understand the impact of slope on variation in net radiation in relation to vegetation density, NSRF was calculated for a range of values on an inclined south facing hillslope. Four different slope angles (0°, 15°, 30°, and 45°) were considered. Since forests are uncommon on very steep hillslopes, the maximum slope angle was limited to 45°. Changes in slope angle influences sky view factor, solar incidence angle (θ), shading fraction, and hence NSRF.
 For all slope angles considered in this experiment, SVF decreases with increasing vegetation density () as expected (Figure 9a). For lower forest densities where the distance between trees is large, the difference in sky view factor for different slope angles is very small. In relatively dense forests ( >0.06 m−1 or cc >10%), as slope increases, the angles subtended by the southern and northern trees increases and decreases, respectively. Since the rate of increase of the subtended angle by the southern trees are larger, sky view factor decreases with increasing slope angle in denser forests. As noted in section 3.1, ↓ Lsky and ↓ Ltree are proportional to SVF and 1 − SVF, respectively. On the other hand, ↑ Lsnow is independent of SVF and hence to slope variations (equation (7)). Since εcrown and εtrunk are greater than εsky, under clear sky conditions, LNet follows the trend of ↓ Lcan and increases with decreasing SVF. As a result, SVF decreases with increase in slope, and LNet increases slightly with increasing slope (Figure 9a). Solar incidence angle (θ) is also influenced by changes in slope. Seasonally averaged θ at noon shows that θ decreases quickly with increase in slope from zero to 30° (Figure 9c, inset). Between slope angles of 30° and 45° (close to the site latitude), θ decreases at a lower rate. Shading fraction also varies with slope. Seasonally averaged shading fraction during daytime hours shows a decreasing trend for higher slopes (Figure 9b, inset). Furthermore, Lpath is also smaller for higher slopes. Since solar incidence angle (θ) and shading fraction are largest for level forests, ↓ Sdir is smallest (equation (8)) for this slope case. Increasing slope therefore increases ↓ Sdir on the south facing hillslope. Since the radiation components are averaged from solstice to solstice, direct shortwave radiation is maximum for slope = 45°, at the modeling site. Furthermore, ↓ Sdif exhibits a decreasing trend with increase in slope (data not shown) because of decreasing SVF and cos(β/2) (see equation (15)). Since the comparative magnitude of ↓ Sdir is more than ↓ Sdif, both ↑ Ssnow and SNet increase with slope (Figure 9b).
 As both SNet and LNet increase with slope, NSRF increases for all vegetation densities with increasing slope. In sparse forests ( < 0.03 m−1 or cc < 3%), NSRF is highest relative to denser forests. On steeper slopes (hill slope angle ≥ 30°), the maximum NSRF occurs for 0.02 m−1 < < 0.03 m−1 (1% < cc < 3%) and is around 5% more than in open areas. The ratio of net radiation at the vegetation density that minimizes SNet relative to radiation at an unforested site increases with slope angle. In forests with hill slopes of 15°, net radiation on the forest floor at ≈ 0.13 m−1 or cc ≈ 47% is about 78% less than the amount in open areas but only about 10% less than in dense forests ( >0.16 m−1). For a slope angle equal to 30°, forests with >0.16 m−1 or cc ≈ 72% are observed to have the minimum NSRF, and increasing vegetation density beyond this point has a negligible effect on NSRF, so this vegetation density effectively represents the point at which NSRF plateaus. The minimum NSRF is about 78% less than net radiation under open conditions. For an even higher slope angle of 45°, minimum radiation is obtained for very dense forests ( > 0.16 m−1) with magnitude of 78% less than NSRF in open areas. The vegetation density at which NSRF is minimized increases steadily from 0.12 m−1 to 0.16 m−1 with increasing slope (Table 3). This is due to a larger increase in SNet than increase in LNet with slopes for sparser tree densities. For very dense forests ( > 0.16 m−1), net shortwave radiation is mainly diffuse and is close to zero, and hence the changes in NSRF with slope in this setting are mostly governed by LNet. LNet in dense forests changes only marginally with different slopes. Hence, NSRF for different slopes are very similar for the highest canopy densities where > 0.16 m−1 (Figure 9c). When sky cloudiness is considered, LNet and SNet show an increasing trend with increasing slope angle, similar to clear sky conditions. Additionally, changes in NSRF with aspect for very sparse forests ( < 0.02 m−1) are larger than changes in very dense forests ( > 0.16 m−1). Since increases in net shortwave radiation with slope are much larger than increases in longwave radiation, NSRF shows a nonmonotonic trend for higher slopes. For higher slopes, in very sparse and very dense forests, the rate of increase in LNet is dominant to the rate decrease in SNet, resulting in a local maximum in low-density and a local minimum in high-density forests. For slope angles of 30° and 45°, although the minimum radiation is still existent for sparse forests, a strong local minimum is exhibited at intermediate vegetation density ( ≈ 0.10 m−1, Figure 9d).
Table 3. Minimum Radiation on Different North and South Facing Slopes
Minimum NSRF Occurs at (m−1)
Proportion of Radiation Relative to Open Area (%)
Proportion of Radia-tion Relative to Very Dense Forest (%)
0° (level forest)
15° south facing
30° south facing
45° south facing
15° north facing
30° north facing
45° north facing
3.4 Effect of Aspect on Radiation
 Variability of NSRF with vegetation density for different aspects was assessed using seven different orientations ranging from 0° to 180°, for a 15° forest slope. For this assessment, 0° indicates a south facing slope, while 180° represents a north facing slope. We note that a 15° slope angle was chosen as a typical mountainous site so that the influence of aspect on variability of NSRF with vegetation density could be demonstrated.
 Aspect does not affect sky view factor; hence, for all aspects, longwave radiation components are the same as for south facing forests (Figure 10a). However, different aspects strongly affect solar incidence angle (θ), Lpath, and hence shading fraction and transmissivity. Increasing both solar incidence angle and shading fraction reduces ↓ Sdir for increasing aspects (Figures 10b and 10c). The minimum ↓ Sdir is observed for the north facing hillslope as would be expected. Since both sky view factor and slope remain unchanged for different hillslope aspects, ↓ Sdif is independent of orientation angle. ↑ Ssnow is proportional to ↓ Sdir + ↓ Sdif, and hence it decreases with increasing aspect. As a result, as aspect angle increases (from 0° to 180°), SNet decreases and exhibits a minimum value for north facing forests as would be expected (Figure 10b).
 Monotonic increasing and decreasing trends of LNet and SNet with again leads to a minimum in NSRF for intermediate forest densities (Table 4). As noted in section 3.3, on a south facing hillslope (slope = 15°), NSRF is minimum for ≈ 0.13 m−1 or cc ≈ 47%. In this case, net NSRF is about 78% less than in open areas but only about 10% less than in dense forests ( > 0.16 m−1 or cc >75%). On hillslopes with an aspect angle, ZS, of 30°, forests with ≈ 0.13 m−1 or cc ≈ 47% have a minimum NSRF that is 77% less than net radiation in open areas and about 10% less than in the dense forests ( > 0.16 m−1) evaluated in this study. As aspect angle increases, the minimum NSRF occurs at lower vegetation densities. In other words, north facing forests have minimum NSRF for sparser tree densities than for south facing forests (Figure 10c). This is because more shortwave radiation is attenuated in sparse forests due to the relatively long path lengths on north facing slopes, whereas the longwave radiation emitted by the forest canopy is controlled by vegetation density and is not affected by aspect. Again, for very dense forests ( > 0.16 m−1), NSRF for different aspects are the same, similar to what has been previously observed [Ellis et al., 2011]. When sky cloudiness is considered, similar to clear sky conditions, increasing aspects lead to decreases in SNet. Since the decrease in SNet is larger for sparser densities, the monotonic increasing trend of NSRF with vegetation density is sustained for all aspects (Figure 10d).
Table 4. Minimum Radiation for Different Aspects
Minimum NSRF Occurs at (m−1)
Proportion of Radiation Relative to Open Area (%)
Proportion of Radiation Relative to Very Dense Forest (%)
0° (south facing)
90°(east or west facing)
180° (north facing)
4 Summary and Conclusions
 A spatially distributed physically based model (FoRM) was run for a simulated white spruce forest stand near Greenville, ME, to develop a general understanding of how net snow cover radiation is sensitive to vegetation density, slope, and aspect in midlatitude coniferous forests. The results showed that in clear sky conditions minimum net radiation on the forest floor is observed for denser forests ( > 0.12 m−1 or cc > 40%) with increasing slope to the south. When sky cloudiness was considered, minimum radiation occurs in open areas and very sparse forests. However, a local minimum is exhibited at an intermediate vegetation density ( ≈ 0.10 m−1 or cc ≈ 28%) for high slope angles (30° and 45°). As the aspect of hillslopes change from south facing to north facing, in clear sky conditions, north facing forests have minimum net radiation for sparser tree densities than that for south facing forests. When sky cloudiness is considered, net radiation increases almost linearly for north facing forests. Additionally, the variation of net radiation with vegetation density when cloudiness is considered is significantly less than that in clear sky conditions.
 The results suggest that appropriate forest management strategies that are aware of local climate factors, may be used to modulate radiation on the forest floor, and hence manage the melt rate of deposited snow. In managed white spruce level forests at ~45°N latitude with a vegetation density of about ≈ 0.12 m−1 equivalent to about 40% canopy closure, net radiation is less than 26% of the amount in open areas (for clear sky conditions) and about 77% of the amount in dense forests ( > 0.16 m−1 or cc > 75%). Results also indicate that lower and higher densities are required to minimize net snow cover radiation on north and south facing slopes, respectively. These results should be used with caution when determining optimal densities to retain snow. Further sensitivity analyses should be performed to evaluate the effect of uncertainties in data and model structure, and in length of the snow season before management strategies are implemented for a specific location.
Appendix A: Calculation of Extraterrestrial Radiation and Solar Angles
 Extraterrestrial radiation for the Nth day of the year is evaluated using [Kalogirou, 2009]
where Sc = 1366.1 W/m2 is solar constant. Solar incidence angle θ, the angle between the Sun's rays and the normal on a surface, is calculated for an inclined slope β with aspect Zs using [Kalogirou, 2009]
where δ is solar declination angle, h is solar hour angle, and L is latitudinal location. Solar declination angle (degree) for the Nth day of the year is calculated by
 Solar hour angle is
where AST is the apparent solar time (minute). Apparent solar time is estimated using
where LST is local standard time (minute), ET is equation of time (minute), SL is standard longitude, LL is local longitude, and DS is day light saving amount (minute). The value of the equation of time is obtained using
 Solar zenith angle (ψ) for the latitude L is approximated by solving
 Solar azimuth angle is evaluated by solving
 This study was supported by the Duke University start-up grant for new faculties, and by NSF-CBET Award 0854553. We also would like to thank Janet Hardy, Cold Regions Research and Engineering Laboratory, and Richard Essery, University of Edinburgh, for providing us the LSOS data.