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**Atmospheric Chemistry and Physics**
An interactive open-access journal of the European Geosciences Union

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- About
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**Research article**
13 Apr 2018

**Research article** | 13 Apr 2018

The influence of idealized surface heterogeneity on virtual turbulent flux measurements

^{1}Institute of Meteorology and Climate Research, Atmospheric Environmental Research (IMK-IFU), Karlsruhe Institute of Technology (KIT), Kreuzeckbahnstrasse 19, 82467 Garmisch-Partenkirchen, Germany^{2}Institute of Geography and Geoecology (IfGG), Karlsruhe Institute of Technology (KIT), Kaiserstrasse 12, 76131 Karlsruhe, Germany

^{1}Institute of Meteorology and Climate Research, Atmospheric Environmental Research (IMK-IFU), Karlsruhe Institute of Technology (KIT), Kreuzeckbahnstrasse 19, 82467 Garmisch-Partenkirchen, Germany^{2}Institute of Geography and Geoecology (IfGG), Karlsruhe Institute of Technology (KIT), Kaiserstrasse 12, 76131 Karlsruhe, Germany

**Correspondence**: Frederik De Roo (frederik.deroo@kit.edu)

**Correspondence**: Frederik De Roo (frederik.deroo@kit.edu)

Abstract

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The imbalance of the surface energy budget in eddy-covariance measurements is still an unsolved problem. A possible cause is the presence of land surface heterogeneity, which affects the boundary-layer turbulence. To investigate the impact of surface variables on the partitioning of the energy budget of flux measurements in the surface layer under convective conditions, we set up a systematic parameter study by means of large-eddy simulation. For the study we use a virtual control volume approach, which allows the determination of advection by the mean flow, flux-divergence and storage terms of the energy budget at the virtual measurement site, in addition to the standard turbulent flux. We focus on the heterogeneity of the surface fluxes and keep the topography flat. The surface fluxes vary locally in intensity and these patches have different length scales. Intensity and length scales can vary for the two horizontal dimensions but follow an idealized chessboard pattern. Our main focus lies on surface heterogeneity of the kilometer scale, and one order of magnitude smaller. For these two length scales, we investigate the average response of the fluxes at a number of virtual towers, when varying the heterogeneity length within the length scale and when varying the contrast between the different patches. For each simulation, virtual measurement towers were positioned at functionally different positions (e.g., downdraft region, updraft region, at border between domains, etc.). As the storage term is always small, the non-closure is given by the sum of the advection by the mean flow and the flux-divergence. Remarkably, the missing flux can be described by either the advection by the mean flow or the flux-divergence separately, because the latter two have a high correlation with each other. For kilometer scale heterogeneity, we notice a clear dependence of the updrafts and downdrafts on the surface heterogeneity and likewise we also see a dependence of the energy partitioning on the tower location. For the hectometer scale, we do not notice such a clear dependence. Finally, we seek correlators for the energy balance ratio in the simulations. The correlation with the friction velocity is less pronounced than previously found, but this is likely due to our concentration on effectively strongly to freely convective conditions.

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De Roo, F. and Mauder, M.: The influence of idealized surface heterogeneity on virtual turbulent flux measurements, Atmos. Chem. Phys., 18, 5059–5074, https://doi.org/10.5194/acp-18-5059-2018, 2018.

1 Introduction

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The interpretation of the turbulent fluxes of latent and sensible heat at the Earth's surface still suffers from the unresolved energy balance closure problem of the eddy covariance (EC) measurement technique. That is, the measured turbulent fluxes are not equal to the available energy at the earth's surface (e.g., Foken, 2008; Leuning et al., 2012). There is an ongoing debate whether the missing energy can perhaps be solely described by additional missing terms related to energy conversion and storage or that the imbalance is a consequence of measurement errors in the velocity measurement due to flow distortion from the sonic anemometer pins. With respect to flow distortion, Horst et al. (2015) quoted an error of maximal 5 % but Kochendorfer et al. (2012) and Frank et al. (2013) claimed an error up to 15 %. In response to the 15 % error, one of us (Mauder, 2013) has pointed out some counter-evidence and a recent modeling study by Huq et al. (2017) on flow distortion did not find evidence for such large errors either. In short, it is unlikely that the previously mentioned issues can explain the fact that very different sites around the world often exhibit an imbalance of more than 20 % (e.g., Wilson et al., 2002; Hendricks-Franssen et al., 2010; Stoy et al., 2013).

In fact, the studies by Mauder et al. (2007) and Stoy et al. (2013) have shown
that a common property among sites that do not close the energy balance is a
more pronounced surface heterogeneity on the landscape-scale. This motivates
us to investigate the energy balance closure problem in the context of
landscape heterogeneity. Moreover, Stoy et al. (2013) also found a good
correlation between the friction velocity (*u*_{*}) and the energy balance
closure. This result was reproduced by Eder et al. (2015b) by means of a study
combining Doppler wind lidar and EC tower data. The same correlation has also
been noticed in a recent year-long large-eddy simulation (LES) by
Schalkwijk et al. (2016) and in an idealized LES study by Inagaki et al. (2006).
In addition, the study of Eder et al. (2015b) could relate the energy balance
residual to the mean gradients in the lower boundary-layer, thereby providing
more evidence for the connection between the energy imbalance and the
presence of quasi-stationary structures in the boundary layer. These
circulations typically arise in heterogeneous terrain but may also develop
over a completely homogeneous surface to a lesser extent, depending on the
atmospheric stability regime, due to self-organization. Persistent updrafts
and downdrafts tied to the landscape heterogeneity have been found e.g., by
Mauder et al. (2010) during the 2008 Ottawa field campaign. In the case of
cellular convection in heterogeneous terrain the distinction between the
primary and the secondary circulation becomes blurred, when the convection
cells are tied to the landscape heterogeneity.

The influence of heterogeneous landscapes on properties of the atmospheric boundary-layer has already been investigated for a few decades with numerical models, primarily large-eddy simulation. We will summarize a few results that are relevant to the non-closure of the energy balance. Avissar and Chen (1993) obtained significant mesoscale fluxes tied to the terrain heterogeneity. These mesoscale fluxes are carried by the vertical wind of the meso-scale circulations, however, they are not present at the ground level. Raupach and Finnigan (1995) also found that surface heterogeneity induces boundary-layer motions, nevertheless the area-averaged properties, including the fluxes, were not significantly influenced by the heterogeneity or the circulation. At the first glance, both statements appear in conflict with a generic influence of the landscape heterogeneity around a measurement site on the energy balance closure.

On the other hand, Shen and Leclerc (1995) found that the horizontally averaged
variances and covariances were influenced by land surface heterogeneity with
scales smaller than the boundary-layer depth. This was also confirmed by
Raasch and Harbusch (2001). This apparent contradiction can be explained by the fact
the resolution of these models was coarse due to computational restrictions
at that time, which has a few implications. Firstly, from continuity we
indeed expect no vertical meso-scale transport by advection with the mean
flow at the lowest grid point representing the lower surface, since *w*=0 due
to the rigid no-slip boundary, but horizontal flux-divergence plays a role,
too. Secondly, we should keep in mind that areally averaging over
sufficiently large distances represents a form of spatial filtering due to
the coarse resolution. Steinfeld et al. (2007) argued that a spatial filtering
method will yield energy balance closure, whereas single-tower temporal
averaging of the sensible heat flux signal in heterogeneous domain suffers
from low-frequency contributions due to the shifted co-spectrum.

In summary, the previously mentioned studies showed that landscape
heterogeneity can induce mesoscale motions in the boundary-layer, especially
for heterogeneity of length scales larger than the boundary-layer height. By
using a large-eddy simulation model coupled to a land-surface scheme,
Patton et al. (2005) investigated strip-like heterogeneities between 2 and
30 km. They found that the heterogeneities with length scales of 4 to 9 km
were the most influential in altering the structure of the boundary-layer. A
similar coupled model approach was used by Brunsell et al. (2011) to study
three heterogeneity scales (approximately 10^{−1}*z*_{i}, *z*_{i}, 10 *z*_{i},
with *z*_{i} the boundary-layer height). They found that only in the surface
layer the length scale of the heterogeneity affected the spectral signature
of the turbulent heat fluxes, and signals appeared blended in the mixed
layer. Still, for the heterogeneity length of 10*z*_{i}, secondary
circulations arising from surface heterogeneity that extend through the whole
boundary-layer were found. Furthermore, Brunsell et al. (2011) found that the
partitioning between latent and sensible heat was affected by the scale of
heterogeneity as the simulations for the intermediate scales led to a higher
Bowen ratio. Since the intermediate scales (of scale *z*_{i}) appear more
heterogeneous than the small or the large scales, this points toward the
dominant influence of the sensible heat flux. Charuchittipan et al. (2014) also
suggested to ascribe a larger fraction of the residual to the sensible heat
flux than to the latent heat flux. The influence of synthetic surface
heterogeneity on the Bowen ratio was also investigated by
Friedrich et al. (2000) who found a non-linear response of the aggregated
Bowen ratio on the underlying land-surface distribution. Bünzli and Schmid (1998)
investigated idealized heterogeneity by means of a two-dimensional *E*−*ϵ* model and found good correspondence with an analytical averaging
scheme based on the context of a numerical blending height.

Although the above findings indicate that surface heterogeneity at scales of
boundary-layer depth and larger can couple to the full boundary layer,
surface heterogeneity at scales considerably smaller than the boundary-layer
height appears to be blended, as observed by Raupach and Finnigan (1995).
Furthermore, Avissar and Schmidt (1998) found that under a mild background wind, the
influence of surface heterogeneity is quickly destroyed in accordance with
the findings of Hechtel et al. (1990). However, Maronga and Raasch (2013), who
performed LES simulations for the response of the convective boundary layer
in realistic heterogeneous terrain, advised that sufficient time and ensemble
averaging is needed to extract the heterogeneity-induced signal, and they
concluded that the upstream surface conditions can still influence the
boundary-layer properties under light winds. Albertson and Parlange (1999) showed
that blending of the surface heterogeneity appears even under convective
conditions, except for very large heterogeneities. However,
Suehring and Raasch (2013) suggest that the blending of the surface follows from
insufficient averaging. Therefore an apparent blending does not necessarily
imply that small-scale surface heterogeneity could not have an influence on
the energy budget at the surface. However, if smaller scales are indeed
completely blended in the mixed layer and therefore do not lead to
circulations that involve the full boundary-layer, then we cannot expect
non-surface layer properties (say, bulk gradients in the mixed layer or
entrainment parameters) to correlate well with the energy balance residual.
Though even in the blended case small scale heterogeneity could still
influence the surface energy budget through motions in the surface layer when
the latter survive half-hour averaging. Indeed, for suburban terrain
Schmid et al. (1990) noted significant differences in energy balance ratios at
scales of 10^{2}–10^{3} m, presumably due to micro-advection between the
patches of different surface type.

Acknowledging the connection between the energy imbalance and
quasi-stationary flow on the one hand, and quasi-stationary flow and surface
heterogeneity on the other hand, we will investigate the effect of surface
heterogeneity on the energy balance closure problem in this work. To this
end, we will study a series of synthetic idealized landscapes that consist of
a chessboard pattern of surface fluxes with different amplitude and
different wavelengths in the *x* and the *y* direction. We will quantify the
average influence on virtual tower data, and investigate the correlation of
the energy balance ratio with surface characteristics, boundary-layer
properties and turbulence statistics. To disentangle the influence of the
surface heterogeneity from that of the meteorology, we will focus on a set-up
of free convection without a synoptic wind (which will effectively lead to
strongly to freely convective conditions diagnosed by the virtual towers). As
hinted to in Brunsell et al. (2011), in heterogeneous terrain the sensible heat
flux appears more important for the imbalance at the intermediate length
scales considered in their work, and we shall therefore focus on simulations
that are practically dry (we have added a very small moisture flux). In
addition, as both the lack of closure and the strength of the circulations
are most pronounced for strongly convective conditions, we will likewise
focus on (effectively) strongly unstable conditions to free convection with
the instability parameter $-z/L$ ranging from 1 to 5000. The $-z/L$ is
different from ∞ because the convective conditions lead to cellular
circulation patterns, which locally induce a friction velocity at the
surface, and due to its positiveness, there will also be a horizontally
averaged *u*_{*} different from zero, as we derive the friction velocity from
the kinematic momentum flux (*τ*_{0}∕*ρ*), in the same manner as how it is
applied in standard eddy-covariance measurements
(e.g., Kaimal and Finnigan, 1994):

$$\begin{array}{}\text{(1)}& {u}_{*}^{\mathrm{2}}={\mathit{\tau}}_{\mathrm{0}}/\mathit{\rho}={\left({\stackrel{\mathrm{\u203e}}{{u}^{\prime}{w}^{\prime}}}^{\mathrm{2}}+{\stackrel{\mathrm{\u203e}}{{v}^{\prime}{w}^{\prime}}}^{\mathrm{2}}\right)}^{\mathrm{1}/\mathrm{2}}\phantom{\rule{0.125em}{0ex}}.\end{array}$$

This definition of friction velocity by the momentum flux is found in general
fluid mechanics as well (e.g., Landau and Lifschitz, 1959). However, only in
homogeneous flow, the friction velocity makes sense as a scaling parameter in
Monin-Obukhov similarity theory. Therefore, we want to stress that when the
friction velocity is derived from the mean velocity gradient, this is only
valid in homogeneous flow. For conditions of free convection in homogeneous
terrain the friction velocity derived from the mean velocity is clearly zero
(even though free convection flow is locally inhomogeneous). As we focus on
heterogeneous flow in our study of heterogeneous terrain, we will make use of
the momentum flux (1) to derive the friction velocity.
From the perspective of the tower measurement, eddy-covariance measurements
alone cannot distinguish if a measured *u*_{*} follows from the wind aloft or
locally from the convection-driven circulation. In addition, the circulation
locally leads to advective terms that can influence the energy balance
closure: e.g., near an updraft there will be horizontal convergence in the
flow field. Even in homogeneous terrain these advective terms can lead to a
non-closure of the surface energy budget (e.g., Kanda et al., 2004). Despite
the issues related to blending, we will focus on heterogeneity of length
scales between 10^{2}–10^{3} m, as for these scales the energy imbalance is
most pronounced. The intermediate scales of *O*(10^{3} m) are of the order
of the boundary-layer depth under typical convective conditions for
mid-latitude afternoons, whereas the smaller scales of *O*(10^{2} m) are of
the order of the surface-layer height. To keep the terminology more general
than typical convection for mid-latitude afternoons, we will refer to them as
heterogeneity of kilometer scale and hectometer scale. According to the
classification of Orlanski (1975) these length scales are at the lower
end of the meso-gamma-scale and at the upper end of the micro-alpha-scale,
respectively. Previous investigations with LES on the energy
budget had been limited to more regular terrain with at least one homogeneous
dimension, see the works of e.g., Kanda et al. (2004), Inagaki et al. (2006),
Steinfeld et al. (2007) or Huang et al. (2008). Typically, the storage term was
subtracted from the surface flux and only the vertical components of the
energy balance were considered: i.e., the turbulent flux and a meso-scale
flux (i.e., vertical advection) arising from turbulent organized structures
(TOS) or heterogeneity-induced meso-scale motions (TMC). On the contrary, we
will also analyze the contribution of the storage flux to the energy
imbalance explicitly. Furthermore, the results presented there hold for the
domain-averaged imbalance and the method used is limited to heterogeneous
terrain with at least one homogeneous dimension. However, in this work we can
extend the analysis of the energy budget to a full budget of the turbulent
fluxes, by including additional terms stemming from horizontal advection by
the mean flow. We take full account of all horizontal and vertical energy
balance components with a so-called control volume approach, as in
Finnigan et al. (2003), Wang (2010), and Eder et al. (2015a). As such, a
study of two-dimensional heterogeneous domains becomes possible.

Let us stress again the research questions of this paper. The first aim is to investigate the average influence on virtual flux measurements of land surface heterogeneity in the form of a variable surface heat flux, for a given length scale of the heterogeneity. We focus on length scales of the order of kilometer, and also on length scales of the order of hectometers. The second aim is to correlate the simulated energy balance ratio to various observables that can be obtained from the simulation output and that are also measurable in a realistic setting.

2 Methods

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For our simulations we have made use of the LES model PALM (Maronga et al., 2015). More precisely, we ran our simulations with PALM version 3.9. PALM resolves the turbulence down to the scale of the grid spacing, all turbulence below is parameterized by implicit filtering. The closure model in PALM is a so-called 1.5-order closure scheme, where the equations for the resolved velocities and scalars are derived by implicit filtering over each grid box of the turbulent Navier–Stokes equations, and where an additional prognostic equation for the turbulent kinetic energy is solved. The turbulent kinetic energy in PALM (the sum of the variance of the subgrid-scale velocities) allows the modeling of the energetic content of the subgrid-scale motions, and because it is related to spatial filtering it should not be confused with the typical turbulent kinetic energy in eddy-covariance measurements related to the averaging of a time series. Of course, the latter can be approximated by the resolved kinetic energy in PALM plus the subgrid-scale turbulent kinetic energy. Finally, the Reynolds fluxes that appear in PALM's filtered equations (the spatial covariances of the subgrid-scale quantities) are parameterized by a flux-gradient approach involving the resolved gradient and a diffusivity coefficient that depends on the before-mentioned turbulent kinetic energy, the grid spacing and the height above the lower surface. However, at the first grid-point above the surface, Monin–Obukhov similarity theory is applied to derive the horizontal velocity and therefore the turbulence there is completely parameterized. It is worth noting that the application of MOST at the first grid point in an LES is done locally and based on the instantaneous velocity.

Relevant parameters of the simulation setup are summarized in
Table 1. The grid spacing is 10 m in all three dimensions and
the domain size is 6×6 km^{2} in the horizontal, and 2.4 km in
the vertical. Demanding that the subgrid-scale flux does not exceed 1 % of
the resolved flux, we will place our virtual flux measurements at 50 m
height. The boundary conditions of the simulations are periodic in the
lateral dimensions. For the velocity we have Dirichlet conditions at the
bottom (i.e., rigid no-slip conditions) with zero vertical and horizontal
wind. At the top the horizontal velocity is commonly set to the geostrophic
wind and the vertical velocity is zero. However, we have turned the
geostrophic wind off (this is a homogeneous horizontal pressure gradient):
$({u}_{\mathrm{g}},{v}_{\mathrm{g}})=(\mathrm{0},\mathrm{0})$. Nevertheless, due to the differences
in surface heating, local pressure gradients will still develop. For
potential temperature and humidity we have Neumann conditions at the lower
boundary (given by the surface fluxes) and also at the top boundary (where
the flux is given by the lapse rate at initialization). The domain is
initialized with constant profiles for the velocity (equal to the geostrophic
wind for *x* and *y* and zero for the vertical velocity). The initial
profiles are homogeneous in *x* and *y* and for potential temperature
(*θ*) it reads as follows:

$$\begin{array}{}\text{(2)}& \mathit{\theta}\left(z\right)=\mathrm{300}\phantom{\rule{0.125em}{0ex}}\mathrm{K}-\mathrm{0.01}\phantom{\rule{0.125em}{0ex}}\mathrm{K}\phantom{\rule{0.125em}{0ex}}{\mathrm{m}}^{-\mathrm{1}}\times \left(z-\mathrm{1}\phantom{\rule{0.125em}{0ex}}\mathrm{km}\right)\times \mathcal{H}(z-\mathrm{1}\phantom{\rule{0.125em}{0ex}}\mathrm{km})\phantom{\rule{0.125em}{0ex}},\end{array}$$

where ℋ(⋅) is the Heaviside function. The top of the domain is situated within a stable inversion layer, which prevents that the turbulence within the boundary-layer is influenced by the vertical domain size. In the lateral dimensions the domain is about 3 to 5 times the boundary-layer depth. For the vertical velocity we have added a very small subsidence term (leading to a vertical pressure gradient in the equations) for heights above 1 km to counteract the destabilizing influence of the surface heat flux, with the subsidence velocity ${w}_{\mathrm{s}}=-\mathrm{0.00003}\phantom{\rule{0.125em}{0ex}}\left(z-\mathrm{1}\phantom{\rule{0.125em}{0ex}}\mathrm{km}\right)\phantom{\rule{0.125em}{0ex}}{\mathrm{s}}^{-\mathrm{1}}$ for all simulations. The data are extracted for four hours after two hours of spin-up time. For each hour a data point is collected by averaging over virtual measurements sampled at every second. As our focus lies on the influence of the surface characteristics, we concentrate in the present study on the wind circulations purely generated by the surface heat flux, without complicating the analysis with additional synoptic drivers such as e.g., a geostrophic wind.

We ran two suites of simulations, one suite with 144 simulated cases focusing
on surface heterogeneity of the kilometer scale (Table 2), and
another suite with 144 simulated cases focusing on surface heterogeneity of
the hectometer scale (Table 3). The simulations are driven by a
spatially variable surface sensible heat flux, the variation of which is
controlled by a few parameters. More precisely, the surface sensible heat
flux *H* at each surface point (*x*,*y*) is determined as follows:

$$\begin{array}{}\text{(3)}& H(x,y)=\left(\mathrm{1}+{A}_{x}\phantom{\rule{0.125em}{0ex}}\mathbb{1}(x/{L}_{x})\right)\left(\mathrm{1}+{A}_{y}\phantom{\rule{0.125em}{0ex}}\mathbb{1}(y/{L}_{y})\right){H}_{\mathrm{0}}\phantom{\rule{0.125em}{0ex}},\end{array}$$

where 𝟙 is a antisymmetric periodic function with period equal to 2, and alternating between −1 and 1, calculated as follows:

$$\begin{array}{}\text{(4)}& \mathbb{1}\left(x\right)=\mathrm{sin}\left(\mathit{\pi}x\right)/\left|\mathrm{sin}\left(\mathit{\pi}x\right)\right|\phantom{\rule{0.125em}{0ex}}.\end{array}$$

The amplitudes of the two-dimensional surface heat flux are given by *A*_{x}
and *A*_{y} and the periods by *L*_{x} and *L*_{y}. *H*_{0} is the average surface
heat flux. In Fig. 2 we show an example of a synthetic surface heat
flux as in Eq. (3) creating eight patches on the surface with
four different values for the surface sensible heat flux. The number of
patches depends on the length scale of the heterogeneity.

The main aim of this parameter study is to find out the response of virtual
towers in heterogeneous terrain of a certain length scale with variable
surface parameters. For this reason we create two suites of simulations where
each simulated case has another combination of the surface parameters. The
surface parameters are the length scales *L*_{x} and *L*_{y} and the amplitudes
*A*_{x} and *A*_{y}. One suite is focused on kilometer scale heterogeneity, the
other on hectometer scale heterogeneity. As the surface heterogeneity is
two-dimensional, the length scale of the surface pattern cannot be exactly
captured by a single number and therefore we concentrate on the order of
magnitude of the length scale, and not on the exact length, thus comprising 4
combinations of length scales (*L*_{x} and *L*_{y}) within the suites of kilometer scale heterogeneity and hectometer scale heterogeneity, respectively. For determining
the average behavior under the varying surface fluxes within the suite, no
weighting is applied to a particular configuration of the parameters, all
amplitudes and length scales under consideration are treated equally. In
Tables 2–3 we have summarized the range of the
parameters that determine the landscape heterogeneity for each simulated
cases within that suite (two suites of 144 simulated cases). The range of the
Obukhov length and boundary-layer height expresses the variation of these
quantities over the range of the parameter space spanned by the cases of the
suite.

Within the domain, we have positioned nine virtual control volumes. These
control volumes are located at functionally different positions with respect
to the surface heterogeneity, as can be seen in Fig. 2. Four of
them are located at the centers of the patches, four others are located on
the borders between the patches, and one is located at the crossing of the
four patches. The four at the center are positioned in a site that is
homogeneous at the site scale, but heterogeneous at the landscape level. The
virtual towers that are located at the borders of the patches are positioned
at a site that is not homogeneous at the site level. For every control
volume around a virtual tower the size is 5×5 grid points in the
horizontal and 5 grid points in the vertical, representing a cube of
(50 m)^{3}. The limits of the control volume are set on the staggered
vector grid. The implementation of the energy balance calculation for the
control volumes follows the method described in Eder et al. (2015a), which
incorporates the approach suggested by Wang (2010). We briefly summarize
the main equation, obtained in two steps; first by spatially averaging over
the control volume, and then by additional temporally averaging over 1 h
intervals:

$$\begin{array}{ll}{\displaystyle}\u2329\stackrel{\mathrm{\u203e}}{H}\u232a& {\displaystyle}=\u2329\stackrel{\mathrm{\u203e}}{{w}^{\prime}{\mathit{\theta}}^{\prime}}\u232a+\sum _{s=\mathrm{1}}^{\mathrm{4}}{\u2329\stackrel{\mathrm{\u203e}}{{\mathit{v}}_{\u27c2}^{\prime}{\mathit{\theta}}^{\prime}}\u232a}_{\mathrm{s}}+\u2329\overline{w}\u232a\u2329\overline{\mathit{\theta}}\u232a+\sum _{s=\mathrm{1}}^{\mathrm{4}}{\u2329{\overline{\mathit{v}}}_{\u27c2}\u232a}_{\mathrm{s}}{\u2329\overline{\mathit{\theta}}\u232a}_{\mathrm{s}}\\ \text{(5)}& {\displaystyle}& {\displaystyle}+\u2329\mathit{\delta}\overline{w}\phantom{\rule{0.125em}{0ex}}\mathit{\delta}\overline{\mathit{\theta}}\u232a+\sum _{s=\mathrm{1}}^{\mathrm{4}}{\u2329\mathit{\delta}{\overline{\mathit{v}}}_{\u27c2}\phantom{\rule{0.125em}{0ex}}\mathit{\delta}\overline{\mathit{\theta}}\u232a}_{\mathrm{s}}+\u2329\int \stackrel{\mathrm{\u203e}}{{\displaystyle \frac{\partial \mathit{\theta}}{\partial t}}}\mathrm{d}z\u232a\phantom{\rule{0.125em}{0ex}}.\end{array}$$

Here *H* denotes the surface heat flux, *x*, *y* and *z* are the Cartesian
coordinates, *w* the wind component in *z* direction, *θ* the potential
temperature, *v*_{⟂} the velocity vector perpendicular to the lateral
faces in the *x**z*- or *y**z*-planes, which are indicated by “*s*” during the
summation over the 4 lateral faces. The angular brackets indicate the spatial
average over a face of the cube, either lateral (“s”), top or ground
surface and the *δ* are the corresponding spatial fluctuations. An
overbar indicates a temporal average and the primes the corresponding
temporal fluctuations. The term on the left-hand side of the equation is the
“true” surface heat flux, whereas the terms of the right-hand side denote
the eddy-covariance flux at the top of the control volume, the horizontal
flux divergence, the vertical and horizontal advection by the mean flow, the
vertical and horizontal dispersive fluxes (Belcher et al., 2012) and the storage
of *θ* in the control volume. The terms of the above formula are
clarified in Fig. 1. A positive sign for the directional fluxes
means that they point outward of the control volume. However, the surface flux is considered positive when the flow is from the surface to the
atmosphere. Where possible, the Gauss–Ostrogradski theorem^{1} has been used to reformulate a divergence within the control volume as
a surface term. Due to the choice of a cuboid aligned with the coordinate
system for the control volume, the control volume energy balance
(5) simplifies further because only the velocity component
perpendicular to the faces remain. The energy balance ratio (EBR) of the
control volume, which represents the amount of closure of the eddy-covariance
measurement with respect to the true surface flux, is given by the following:

$$\begin{array}{}\text{(6)}& \mathrm{EBR}={\displaystyle \frac{\u2329\stackrel{\mathrm{\u203e}}{{w}^{\prime}{\mathit{\theta}}^{\prime}}\u232a}{\u2329\stackrel{\mathrm{\u203e}}{H}\u232a}}\phantom{\rule{0.125em}{0ex}}.\end{array}$$

From a control volume point of view the net fluxes through the faces are what
balances the storage term inside the volume, and in this manner advection
effects are automatically included in the energy balance of the volume. Of
course, in analogy with measurements, the fluctuations at the top face yield
the “virtually measured” turbulent heat flux: first the temporal
correlations are calculated, then a spatial average over the upper face of
the volume is calculated. The latter average improves the statistical
significance of the virtual measurement. Although the subgrid fluxes become
small at the height of the control volume, we nevertheless include the
vertical component of the subgrid flux into the turbulent heat flux. In this
manner we can also capture the highest-frequency correlations. Real data from
measurement towers is usually sampled up to 10–50 Hz, whereas for
computational efficiency our simulation advances with a time step of one
second, i.e., our simulated data is obtained at 1 Hz. A higher sampling
frequency would not resolve the turbulence better, as the resolution of the
latter is limited by the grid spacing. The part of the total turbulent flux
that is not captured directly by the resolved turbulent flux by 1-Hertz
sampling is transported by the subgrid turbulent flux. For the advective
components we have made a distinction between advection due to the mean flow
versus advection due to the horizontal flux-divergence. In complex terrain we
do not know a well-defined choice of reference for the base temperature, in
contrast to the base temperature in homogeneous terrain that appeared in
Webb et al. (1980). Therefore we have avoided introducing a base temperature
altogether by adding up the advection by the mean flow components, this means
that our advection term is the sum of the horizontal and vertical advection
by the mean flow. The virtual measurement height is quite high, but this is
due to the vertical resolution and the need for sufficient grid points in the
vertical direction to suppress the influence of the subgrid-fluxes whence the
turbulence becomes sufficiently resolved. For the integration of the
temperature in the storage term we apply numerical integration with the
midpoint rule, which assumes a piecewise constant interpolation function.
PALM uses implicit filtering, where it is by construction assumed that the
prognostic variable within the grid cell is the volumetric mean of the
variable over the domain of the grid cell, therefore the midpoint rule is the
most appropriate, because by definition the LES computed *θ*[*k*] is not
*θ*(*z*=*z*_{k}) but instead is as follows:

$$\begin{array}{}\text{(7)}& \mathit{\theta}\left[k\right]=\underset{{z}_{k}-\mathrm{d}z}{\overset{{z}_{k}+\mathrm{d}z}{\int}}\mathit{\theta}\left(z\right)\mathrm{d}z\phantom{\rule{0.125em}{0ex}},\end{array}$$

with *z*_{k} the height of the grid point *k*, d*z* the grid spacing and
*θ* the potential temperature, and we have suppressed the indices *i**j*
for clarity. In this way, the summation of the LES computed discrete profile
values is defined to be equal to the integration of the continuous profile:

$$\begin{array}{}\text{(8)}& \sum _{k=\mathrm{1}}^{K}\mathit{\theta}\left[k\right]=\underset{\mathrm{0}}{\overset{{z}_{\mathrm{m}}}{\int}}\mathit{\theta}\left(z\right)\mathrm{d}z\phantom{\rule{0.125em}{0ex}},\end{array}$$

with the measurement height ${z}_{\mathrm{m}}={z}_{K}+\mathrm{d}z$.

3 Results and discussion

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We start our analysis with a discussion of the location of the updrafts and
downdrafts in heterogeneous terrain. For this purpose, we concentrate on a
few specific cases, more precisely ${A}_{x}={A}_{y}=\mathrm{0.3}$ and all four
heterogeneity lengths (with *L*_{x}=*L*_{y}). We will take the mean vertical
velocity as the simplest proxy for circulation patterns in the boundary
layer. In Fig. 3 we show the time-averaged vertical velocity at the
height of the control volumes (50 m). We stress that the structures at 50 m
extend into the mixed layer above where the absolute velocities become larger
(not shown). The reason for the additional time average (over the complete
virtual measurement interval of 4 h) of the hourly mean data is to
remove the drift of the turbulent structures. Due to the absence of a
background wind, significant circulation patterns can emerge in the
homogeneous case as well. With even longer averaging times a zero mean can be
achieved for idealized simulations in homogeneous terrain, but in a real
atmospheric boundary-layer this is not possible due to non-stationarity on
those timescales. Ensemble averaging is an alternative for time averaging and
our average over the suite removes random turbulence in the individual
realizations.

We notice that for the heterogeneity lengths of *O*(km), the motions within
the mixed-layer clearly reflect the surface pattern, with updrafts
concentrated above the hotter patches and downdrafts above the lower patches
in the 3 km heterogeneity length and a little offset in case of the 1.5 km
heterogeneity length. However, the structure of the convective turbulence for
both kilometer scales are clearly different from homogeneous control run,
where typical cellular convection patterns arise (Schmidt and Schumann, 1989), though
the hectometer scales are qualitatively rather similar to the homogeneous
run. The latter could be a consequence of the blending height. Investigating
the heterogeneity lengths of *O*(hm) with more horizontal detail for the
time-averaged *w*, we do not see clear updrafts or downdrafts tied to the
surface heterogeneity. However, in this respect it could be interesting to
note that some of the hourly mean vertical velocity (without additional
time-average) for the *O*(hm) appears better related to the surface structure.
Similar results appear for weaker amplitudes and also when *A*_{x} is different
from *A*_{y}, in which case the dominant pattern is visible along the direction
with the larger amplitude (not shown). We can conclude that circulations are
tied to the landscape heterogeneity when it is *O*(km). For *O*(hm)
such a correspondence is unclear. However, the latter could be related to the
“coarse” grid resolution and the distance from the ground. Indeed,
Mauder et al. (2010) found persistent updraft and downdraft regions during the
2008 Ottawa field campaign.

On the topic of circulations driven by a surface conditions that are by
design freely convective, we investigate how the domain average of *u*_{*} is
influenced by the surface heterogeneity. The ratio between the surface flux
at the hottest patch and the surface flux at the coolest patch is given by the following equation:

$$\begin{array}{}\text{(9)}& r=\left(\mathrm{1}+{A}_{x}+{A}_{y}+{A}_{x}\cdot {A}_{y}\right)\times {\left(\mathrm{1}-{A}_{x}-{A}_{y}+{A}_{x}\cdot {A}_{y}\right)}^{-\mathrm{1}}\phantom{\rule{0.125em}{0ex}}.\end{array}$$

The horizontal mean of the friction velocity scales very well with the natural logarithm of the following ratio:

$$\begin{array}{}\text{(10)}& {u}_{*}=-\mathrm{0.046}\phantom{\rule{0.125em}{0ex}}\mathrm{ln}\left(r\right)+\mathrm{0.384}\phantom{\rule{0.125em}{0ex}}\phantom{\rule{0.125em}{0ex}},\phantom{\rule{0.125em}{0ex}}{R}^{\mathrm{2}}=\mathrm{0.85}.\end{array}$$

The remaining spread in *u*_{*} does not result from the time stamp or the
heterogeneity length scale. The monotonous decrease of *u*_{*} in function of
the heterogeneity ratio shows that for more homogeneous terrain we will
obtain a slightly larger domain averaged *u*_{*}.

In Fig. 4, we look at the response of the towers with respect to their location, corresponding to the simulations summarized in Table 2. This is the average of the simulation output belonging to the suite of kilometer scale heterogeneity. In this manner, we investigate the average effect of surface heterogeneity of kilometer scale. The towers are ordered according to the available energy at their location, for our model setup the available energy is equal to the surface flux. For each tower we have plotted the energy balance residual (available energy minus the turbulent flux), the advection component from the mean flow, the flux-divergence and the storage flux, all normalized by the available energy at the respective tower, with the plot on the left collecting the towers located in the centers of the patches and the plot on the right collecting the towers located at the borders of the patches. The normalized turbulent flux is effectively the energy balance ratio (EBR), but we show the non-closure (1−EBR), i.e., the normalized energy balance residual, as the latter's magnitude is of the same size as the remaining components. The normalized fluxes in Fig. 4 are also averaged for all the available data points of the respective tower. That is, we averaged over the data with different time stamps and also over all cases within the suite corresponding to the kilometer length scale: this entails $(\mathrm{6}\times \mathrm{6}-\mathrm{1})$ variations of the surface flux amplitudes (we do not count the case where both amplitudes are zero, ${A}_{x}={A}_{y}=\mathrm{0}$, as this is a homogeneous run) multiplied by 2×2 variations of the heterogeneity length, as expressed in Table 2. The error bars on the normalized fluxes denote the spread on the virtual measurements of each tower with respect to the suite. The spread is naturally quite large, as different amplitudes for the surface heat flux pattern are considered at each tower.

To analyze the tower response in more detail, we have separated the towers at the centers (left panel) from those at the borders (central panel). We notice that most towers show the typical underestimation of the energy balance (i.e., positive energy balance residual), except for the tower located at the warmest spot where there is an updraft. In fact, the closed energy balance for the tower in the warm patch is similar to a result in Eder et al. (2015a) where the energy balance was closed for the site with a pronounced updraft. The residual clearly depends on the location of the tower: towers located at the centers of the patches are located in a more homogeneous environment and they exhibit remarkably smaller residuals, as expected. Towers at the borders have up to 10 % more imbalance than the adjacent towers in the center. The tower on the corner of the four patches has the lowest mean closure of only 69 %. For towers located in the centers, it is evident that the tower sites are locally homogeneous but there is still a clear imbalance. As a consistency check, we note that the similar towers (the two towers in the center of the patches with same surface heating; the two sets of two towers on the borders between patches of similar surface heating) behave similarly. We present some arguments why the regions with updrafts have better closure. Banerjee et al. (2017) investigated the dependence of the aerodynamic resistance on the atmospheric stability for homogeneous terrain. As a consequence a surface with a higher surface heat flux is more efficient in transporting away the surface flux. Therefore, one hypothesis is that when a patch with higher surface flux is coupled to a patch with lower surface flux in heterogeneous terrain, the patch with the higher surface flux transports part of the surface flux of the patch with the lower surface flux, due to its higher efficiency, leading to a net advection of sensible heat from the downdraft region to the updraft region. Another hypothesis is that the shape of the cellular convection cells matters: the updrafts cover a smaller area than the downdrafts. Therefore, as the turbulence structures move across the towers, above a region with preferential updrafts, the likelihood of sampling both the updrafts and downdrafts is higher than above a region with preferential downdrafts.

In the right panel, we show the data from four homogeneous control runs (with data extraction window and data selection in the same manner as for the heterogeneous runs). Each of these simulations has nine towers as well, but now all towers have the same surface properties. The mean residual (under-closure) of the homogeneous control runs is around 10 %, less than for the heterogeneous cases but not negligible. There is significant spread on the results, but the residual is mainly composed of advection and storage. Compared to the towers at the edges (middle panel), which are locally heterogeneous, the homogeneous case is clearly different. Compared to the towers at the centers of the patches (left panel), the homogeneous case has a different average but the difference is still within the spread. It is remarkable that flux-divergence is very small in the homogeneous case, in contrast to the heterogeneous terrain. The negligible flux-divergence for a homogeneous site was also apparent in the desert site of Eder et al. (2015a).

As the residual is formed by the sum of advection by the mean flow, storage
and flux-divergence, we now turn our attention to these flux components. It
turns out that primarily the advection by the mean flow determines the
different residuals, but that the flux-divergence has to be taken into
account as well for the full picture. In addition, the storage flux also
plays a role, but its signature is independent on the location of the tower,
and it is always small, which is understandable for our type of surface
conditions: there is only a storage flux due to the heating of the air inside
the control volumes. For different towers, the allocation of the residual to
advection by the mean flow versus flux-divergence varies. At first the
behavior of the flux-divergence appears irregular. Let us however take a
closer look in Fig. 5, where the flux-divergence and advection by
the mean flow, respectively, are plotted against the energy balance ratio. As in
Fig. 4 flux-divergence and advection are normalized by the
available energy (i.e., the surface flux in our settings). In the left panel
of Fig. 5 we note that the normalized flux-divergence correlates
rather well to the normalized turbulent flux, when we look at their average
behavior at each tower. For the individual data points the correlation is
nevertheless scattered (not plotted). It is somewhat remarkable that both the
towers at the center and those at the borders exhibit a similar average
behavior. Indeed, the linear regression is very satisfactory when fitting the
*B*-type towers and the *C*-type towers together. We could have made two
separate fits, one for each tower type as in Fig. 4, but with only
three or four towers of different functionality a linear regression through those
three
or four points would carry less meaning than considering all nine virtual towers
together. If we repeat this linear regression for the advection by the mean
flow versus the energy balance ratio we see that the linear correlation fits
even better (Fig. 5, right panel) but that it has opposite slope.
We had expected that the sum of both components would correlate very well with the
energy balance ratio, since the storage is small and constant, but it is an
interesting result that the flux-divergence and advection also separately
correlate well with energy balance ratio, and consequently, also with each
other.

Finally, we want to remark that due to computational constraints, the
virtual measurement height in our simulations lies at 50 m, which is an
order of magnitude larger than the typical tower height over short vegetation
with comparable surface roughness. This means that our findings for virtual
EC towers cannot be directly transferred to real eddy-covariance towers.
Other LES studies of the energy balance closure point towards a larger
imbalance at higher *z*-levels, e.g., Steinfeld et al. (2007),
Huang et al. (2008), and Schalkwijk et al. (2016). It remains an open question if
we can scale the measurement height (as long as it is in the constant flux
layer) with the boundary-layer depth and the scale of the heterogeneity. We
also analyzed the variation of EBR in function of the surface amplitudes
(*A*_{x} and *A*_{y}) but did not find any clear dependence there.

In Fig. 6 we repeat the foregoing analysis for the landscape
heterogeneity of hectometer scale, with the parameters in the suite now
corresponding to those of Table 3. The difference between the
towers is much less pronounced here compared to the kilometer scale.
Furthermore, the towers in the center of the patches even behave in the
opposite manner when the kilometer and hectometer scales are compared.
Indeed, for the hectometer scales the cooler patches have a smaller residual,
hence better energy balance closure, up to even a mean over-closure for the
tower in the coolest patch, whereas the energy balance at the hottest patch
is not closed. Another example of the opposite behavior is shown by the
flux-divergence. In Fig. 5 it is positively correlated with the
normalized residual and in Fig. 7 we notice that the
flux-divergence is now indeed anti-correlated with the EBR. The advection by
the mean flow is again anti-correlated with the EBR, as it was for the
kilometer scale. The storage is again roughly constant for all towers. The
likely cause for the different behavior between the two scales of
heterogeneity would be the blending of the hectometer landscape
heterogeneity,
due to the virtual tower heights of 50 m. For the surface heterogeneity of
*O*(10^{2} m), the flux footprint of each of the towers can cover
several of the surface patches, regardless of the type of tower. In the right
panel of Fig. 6 we show the data from four homogeneous control
runs. Except for the flux-divergence, the tower responses in heterogeneous
terrain of hectometer scale heterogeneity look similar to the tower responses
of the homogeneous runs.

We investigate the possible connection between the energy balance ratio, the different flux contributions and variables such as friction velocity and boundary-layer height. We performed a linear correlation analysis between these variables and the energy balance ratio. We made one restriction on the data set, which is to limit the boundary-layer depth to values larger than 1 km, thereby excluding about 8 % of the data, in order to obtain a better representation of the boundary-layer depth (when the boundary-layer depths smaller than 1 km are included, the correlation deteriorates).

We found that friction velocity and boundary-layer depth cluster are
well-correlated with each other, but not with EBR. Although we might have
supposed that higher boundary-layer heights will arise if patches are present
with vigorous surface heating. However, we found that *u*_{*} decreased with
stronger surface heterogeneity. Closer analysis reveals that the highest
boundary layer heights are obtained when the heterogeneity amplitudes are
smaller and the domain is more homogeneous. Hence the former clustering can
be explained, as in our scenario with varying heterogeneity amplitudes
the highest boundary-layer height and larger *u*_{*} are both obtained for
smaller heterogeneity amplitudes. Though advection and flux-divergence
correlate well with EBR, they cannot be measured independently and therefore
cannot be used as independent predictors. In the literature
(e.g., Stoy et al., 2013; Eder et al., 2015b) a correlation between friction velocity
and energy balance closure has been found: a high friction velocity leads to
a smaller residual. Typically, a higher friction velocity is correlated to
smaller atmospheric instability and hence roll-like convection instead of
cellular convection. Maronga and Raasch (2013) found that boundary-layer rolls
“smear out” the surface heterogeneity, leading to an effective surface that
looks less heterogeneous, which has been related to a higher EBR
(Mauder et al., 2007; Stoy et al., 2013). Therefore, a possible cause for the present low
correlation of *u*_{*} with the EBR could be our range of the stability
parameter. For the free convective cases considered here, the stability
parameter lies below the range where the friction velocity has a high
correlation with EBR.

The linear correlation analysis shows that the simulated EBR does not linearly depend on easily measured characteristics. As we have learned from Fig. 5, there can be a good fit between the parameter-averages of two variables, e.g., normalized flux-divergence and energy balance ratio average, despite the fact that the individual data points do not correlate as well. This highlights the importance of testing parameterizations for the energy balance closure problem on the level of a data ensemble, instead of parameterizing on the level of the individual hourly measurements.

4 Conclusions

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In this work, we have investigated the effect of idealized surface
heterogeneity on the components of the surface energy budget measured at
virtual measurement towers, by means of large-eddy simulation. By means of a
control volume approach, we have decomposed the modeled surface energy budget
to highlight its partitioning, and we have shown that the modeled energy
balance ratio exhibits values that are found in field experiments. In
addition, this approach allows us to investigate the energy balance closure
in two-dimensional complex terrain. We have found that for surface
heterogeneity with length scale of order kilometer, there is a clear relation
between the energy budget components and the location of the tower with
respect to the patches of surface heterogeneity. For surface heterogeneity of
hectometer scale, the response of the different towers appears to depend to a
lesser extent on their respective location. Towers located at the borders
between patches with different surface heat flux have worse closure than
towers located in the center of a patch. Although storage terms are not
negligible, the size of the residual depends mostly on the advection and
flux-divergence terms. Remarkably, flux-divergence and advection by the mean
flow separately correlate very well with the energy balance ratio, which
implies that the EBR can be explained by the advection or flux-divergence
only, as the latter two are well correlated among themselves. For the
kilometer scale heterogeneities, advection by the mean flow and
flux-divergence behave in opposite ways, while they are positively correlated
for hectometer scale heterogeneities. We did not find a high correlation
between the friction velocity and energy balance ratio but this could be due
to the limited range of *u*_{*} as we have investigated free convection.

Data availability

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Data availability.

Please contact the authors directly for the data.

Appendix A: Example of the heterogeneity length scale of a field site

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Even though the focus of this study is on virtual flux measurements, we can look at an example of a real EC measurement site to make a qualitative comparison of these virtual tower measurements with real tower measurements. In a first approximation, the heterogeneity of the landscape around a measurement site can be characterized by the dominant length scale of a suitable surface variable. In Eder et al. (2014), the dominant length scales corresponding to a few sites belonging to the TERENO measurement network (Zacharias et al., 2011) were computed from the Fourier spectrum of the surface roughness. The site with the least pronounced topography, the site Fendt, has an effective length scale close to 3 km and a mean EBR of 0.77, which is a typical value for the energy balance ratio (Stoy et al., 2013). The location of the measurement tower in Fendt would correspond to a tower of the central type and due to its location in the meadow with lower albedo than the forest or the small built-up area we would assign it to the central tower of the cooler patch. However, the Fourier spectrum of the sensible heat flux may differ from that of the surface roughness. Moreover, the Fourier spectrum for the TERENO site in Fendt exhibits an additional local maximum in its Fourier spectrum of the surface roughness, at 600 m (Fabian Eder, personal communication, 2015). Additionally, it should be noted that even a simplified version of the landscape heterogeneity of Fendt would appear primarily strip-like, in contrast the synthetic chessboard pattern here. The EC tower of Fendt is located in a large north–south oriented meadow which is flanked by two forests further away to the west and the east. Despite these apparent differences between our idealized simulations and the real situation at the Fendt site, the EBR of 0.77 is comparable to the EBR of the virtual towers investigated here for the kilometer heterogeneity.

Competing interests

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Competing interests.

The authors declare that they have no conflict of interest.

Acknowledgements

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Acknowledgements.

We thank the anonymous reviewers for their detailed comments and insightful
remarks, which significantly improved the quality of this work. This work was
conducted within the Helmholtz Young Investigators Group “Capturing all
relevant scales of biosphere-atmosphere exchange – the enigmatic energy
balance closure problem”, which is funded by the Helmholtz-Association
through the President's Initiative and Networking Fund, and by KIT. We thank
the PALM group at Leibniz University Hanover for their open-source PALM code
and their support.

The article processing
charges for this open-access

publication were covered by a
Research

Centre of the Helmholtz
Association.

Edited by: Heini Wernli

Reviewed by: two anonymous referees

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The
Gauss–Ostrogradski theorem or “divergence theorem” is a special case of
the Stokes–Cartan theorem in differential geometry. For our purposes, we also
restrict ourselves to three-dimensional space. We consider a compact volume
*V* with a piecewise smooth boundary *S*. If ** F** is a continuously
differentiable vector field defined on a neighborhood of

$$\begin{array}{}\text{(11)}& \underset{V}{\int}\left(\mathbf{\nabla}\cdot \mathit{F}\right)\phantom{\rule{0.125em}{0ex}}\mathrm{d}V=\underset{S}{\oint}\mathit{F}\cdot \mathrm{d}\mathbf{S}\phantom{\rule{0.125em}{0ex}}.\end{array}$$

The left side is a volume integral of the divergence of the vector field
** F** over the volume

Short summary

We investigate the mismatch between incoming energy and the turbulent flux of sensible heat at the Earth's surface and how surface heterogeneity affects this imbalance. To resolve the turbulent fluxes we employ large-eddy simulations. We study terrain with different heterogeneity lengths and quantify the contributions of advection by the mean flow and horizontal flux-divergence in the surface energy budget. We find that the latter contributions depend on the scale of the heterogeneity length.

We investigate the mismatch between incoming energy and the turbulent flux of sensible heat at...

Atmospheric Chemistry and Physics

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