the Creative Commons Attribution 4.0 License.
the Creative Commons Attribution 4.0 License.
Accounting for meteorological biases in simulated plumes using smarter metrics
Pierre J. Vanderbecken
Joffrey Dumont Le Brazidec
Alban Farchi
Marc Bocquet
Yelva Roustan
Élise Potier
Grégoire Broquet
In the next few years, numerous satellites with highresolution instruments dedicated to the imaging of atmospheric gaseous compounds will be launched, to finely monitor emissions of greenhouse gases and pollutants. Processing the resulting images of plumes from cities and industrial plants to infer the emissions of these sources can be challenging. In particular traditional atmospheric inversion techniques, relying on objective comparisons to simulations with atmospheric chemistry transport models, may poorly fit the observed plume due to modelling errors rather than due to uncertainties in the emissions.
The present article discusses how these images can be adequately compared to simulated concentrations to limit the weight of modelling errors due to the meteorology used to analyse the images. For such comparisons, the usual pixelwise ℒ_{2} norm may not be suitable, since it does not linearly penalise a displacement between two identical plumes. By definition, such a metric considers a displacement as an accumulation of significant local amplitude discrepancies. This is the socalled double penalty issue. To avoid this issue, we propose three solutions: (i) compensate for position error, due to a displacement, before the local comparison; (ii) use nonlocal metrics of density distribution comparison; and (iii) use a combination of the first two solutions.
All the metrics are evaluated using first a catalogue of analytical plumes and then more realistic plumes simulated with a mesoscale Eulerian atmospheric transport model, with an emphasis on the sensitivity of the metrics to position error and the concentration values within the plumes. As expected, the metrics with the upstream correction are found to be less sensitive to position error in both analytical and realistic conditions. Furthermore, in realistic cases, we evaluate the weight of changes in the norm and the direction of the fourdimensional wind fields in our metric values. This comparison highlights the link between differences in the synopticscale winds direction and position error. Hence the contribution of the latter to our new metrics is reduced, thus limiting misinterpretation. Furthermore, the new metrics also avoid the double penalty issue.
 Article
(3832 KB)  Fulltext XML
 BibTeX
 EndNote
Nearrealtime monitoring of atmospheric gaseous compounds at the scale of power plants, cities, regions, and countries would allow decisionmakers to track the effectiveness of emission reduction policies in the context of climate change mitigation (Horowitz, 2016) or other voluntary emission reduction efforts. Inventories of the emitted atmospheric gaseous compounds are diverse in scale (JanssensMaenhout et al., 2019; Kuenen et al., 2014) and methodology. The elaboration of comprehensive inventories generally combines various approaches based on a complex mixture of measurement techniques, database elaboration, and numerical modelling. Despite the use of quality assurance and control verifications (Calvo Buendia et al., 2019a, b), the emissions fluxes can bear large uncertainties, depending on the species, on the countries or on the spatial scale (Cai et al., 2019; Hergoualc'h et al., 2021; Meinshausen et al., 2009; Pison et al., 2018; Solazzo et al., 2021). Furthermore, the delay between the emissions and the release of the corresponding inventory could be important due to a large amount of data to gather and aggregate. Even when the inventories are known to be accurate, they currently do not fulfil the need for realtime monitoring of emissions at a regional scale. By observing from space the plumes of gases downwind of large cities and industrial plants, and atmospheric signals at a scale of a few to several hundreds of kilometres, the new generation of highresolution satellite imagery may help address this need (Veefkind et al., 2012; Broquet et al., 2018). For instance, the future Copernicus Anthropogenic Carbon Dioxide Monitoring (CO2M) mission will provide images of CO_{2} concentrations at a resolution of almost 2 km^{2}, which will enable the observation of urbanscale pollutant plumes (Brunner et al., 2019; Kuhlmann et al., 2019, 2020). These new images can be directly used through fast methods to quantify the mean emissions of sources (Varon et al., 2018, 2020; Hakkarainen et al., 2021). These fast methods only require images to estimate the emissions. They do so either by using a simplified chemical transport model (CTM) or by averaging the emissions of a given source.
Here we focus on the use of such images to update the emissions sources on a smaller timescale. This can be done using an inverse method relying on comparisons between the images and the predictions of a CTM. A better match between the observed concentration fields and the simulated one will result from a more accurate source. However, the CTM prediction is bounded by the meteorological conditions used. It takes as inputs temperature, pressure, winds, cloud cover fields, etc. Usually, these atmospheric fields are provided by predictions previously obtained with mesoscale numerical weather prediction models (Lian et al., 2018). The estimated atmospheric fields come with uncertainties, which in turn yield uncertainties in the simulated concentration fields, for instance, the location or the main direction of the plume. Within the retrieval algorithm, the concentration fields derived from satellites and CTM models are usually compared pixelwise. However, pixelwise comparison cannot easily remove the relative weight of the meteorological uncertainties within the comparison between observation and simulation. This results in estimated increments applied to the emissions inventories that are biased by the approximated meteorology used in the simulations. This issue is also present in other simulations with observation comparisons (Dumont Le Brazidec et al., 2021; Farchi et al., 2016; Keil and Craig, 2007). Assuming that the temporal variability (e.g. annual cycle, seasonal cycle, diurnal cycle) of the emissions is wellknown and that the CTM is perfect, the displacement between the observed and simulated plumes is driven by the meteorological conditions. Such a displacement yields a position error in the inversion. Thus our main goal is then to define a metric for the comparison that levels down the position error to reduce the weight of meteorology uncertainties within the inversion.
A better account of position error for observation versus simulation comparison of coherent features is a subject of active research (e.g. Ebert and McBride, 2000; Ebert, 2008; Gilleland et al., 2009; Gilleland, 2021). These authors developed several metrics and skill scores that are more sensitive to pathological situations where usual metrics provide less information, especially when there is a position error between the feature they observed and the one forecasted. To do so, they build indicators by splitting the sources of discrepancies and by doing comparisons on deformed meshes (Hoffman et al., 1995; Hoffman and Grassotti, 1996; Amodei et al., 2009; Marzban and Sandgathe, 2010; Gilleland et al., 2010). We will follow the same methodology, by splitting the different sources of discrepancies, but the position errors will include errors due to a translation and a rotation. We will consider a specific class of deformations to free the comparison from position errors. We will consider either (i) an isometric transformation or (ii) a transport map resulting from optimal transport, both differentiable with respect to the compared plumes. Optimal transport metrics were already used for radionuclide plumes (Farchi et al., 2016), but there were computation limitations. To allow a more systematic comparison between the metrics, we use the Kantorovich standpoint on optimal transport.
The objective of this paper is to develop a simple and efficient metric for urbanscale plume images which can level down the difference due to the meteorology while fitting into an inverse framework (following Feyeux et al., 2018; Tamang et al., 2022). Even though the methods could be used for other gaseous compounds, reactive atmospheric gaseous compounds have a more complex transport due to chemistry. For the sake of simplicity, we will consider CO_{2} since it is a passive tracer. Several metric candidates are introduced and compared. From the baseline local ℒ_{2} norm, a new metric with an upstream nonlocal correction of position errors is described in Sect. 2. In Sect. 3, going further away from the local comparison, we use the optimal transport theory to define the Wasserstein distance between two plumes and then to build a new metric freed from position errors. The different metrics are then evaluated and compared on a database of analytical twodimensional Gaussian puff cases in Sect. 4. The metrics are then compared on a realistic database of CO_{2} plumes from a German power plant in Sect. 5. For both databases, the images and the simulations are computed using the same model, which allows us to monitor the discrepancies seen by the metrics. In Sect. 6 we describe the dependence of the four metrics on meteorology, before concluding in Sect. 7.
In this section, we start by introducing the notation in Sect. 2.1 and then the Gaussian puff model used to simulate the plumes in the analytical experiments in Sect. 2.2. Furthermore, we assume that the plumes are already detected and separated from the background noise and instrumental noise. These steps bring challenges that are outside the scope of this article. The ℒ_{2} norm is then defined in Sect. 2.3, with an emphasis on the double penalty issue. To deal with the double penalty issue associated with the family of pixelwise metrics such as the ℒ_{2} norm, a second metric is proposed in Sect. 2.4.
2.1 Discrete and continuous representation of an image
In the present article, we focus on twodimensional images of the enhancement of the total column of CO_{2} concentration or of the groundlevel concentration. These images are given with a discretisation of N pixels. An image can hence be represented by a vector $\mathit{x}={\left({x}_{\mathrm{1}},\mathrm{\dots},{x}_{N}\right)}^{\top}\in {\mathbb{R}}^{N}$.
It is also possible to obtain a continuous representation of the image using interpolation (e.g. bilinear). In this case, the image is represented by a twodimensional field $X:\mathbb{E}\to \mathbb{R}$ defined on a finite domain 𝔼⊂ℝ^{2}. Without loss of generality, we can assume that $\mathbb{E}=[\mathrm{0},\mathrm{1}{]}^{\mathrm{2}}$. Furthermore, the twodimensional field X can be extended to ℝ^{2} by using zero padding outside the original domain 𝔼. If needed, a smooth transition from X to 0 can be included to avoid a sharp gradient at the boundaries of the original domain 𝔼.
For each metric definition, we will use either the discrete or the continuous representation of the images, but this will be explicitly mentioned.
2.2 Analytical plumes
Our Gaussian puff model is a simplified model of a concentration field (e.g. concentration at a given altitude or total column concentration in specific conditions). It has the advantage of yielding analytical expressions for the Wasserstein metrics (see Sect. 3). It is also a relevant case in transport modelling: the transport of a threedimensional Gaussian puff is a simplified model to estimate the transport of nonreactive pollutants (Korsakissok and Mallet, 2009; Seigneur, 2019). A set of Gaussian puffs is used extensively in the following sections to illustrate and evaluate the metric candidates.
In the Gaussian puff model, we assume that X is proportional to the probability density function (pdf) of the normal distribution 𝒩(μ,Σ):
where μ and Σ are the mean and the covariance matrix, respectively. The operator $.$ is the determinant for square matrices. Also, note that since the covariance matrix Σ is positive definite, it can be factored as follows:
where R(θ) is the rotation matrix of angle θ, the angle between the principal axis of the Gaussian and the x axis, and where Δ is a diagonal matrix with the variance along the two principal axes of the Gaussian. Two examples of puffs based on the Gaussian puff model are provided in Fig. 1b and c.
2.3 The ℒ_{2} norm and the double penalty issue
To compare two concentration fields, one can see to what extent the fields overlap. This provides a pixelwise (i.e. local) assessment of the discrepancies. The ℒ_{2} norm is then defined as the sum of the squared discrepancies. More specifically, the ℒ_{2} norm d between two concentration fields X_{A} and X_{B} is defined as
or
in the discrete case, where x_{A} and x_{B} are the two concentration vectors corresponding to the concentration fields X_{A} and X_{B}. In the limit of a higher and higher resolution, the discrete formulation should converge towards the continuous formulation.
To identify the origin of the discrepancies, Feyeux et al. (2018) propose to split the difference between two fields into two categories: the position error and the amplitude error. A position error occurs when the two compared plumes are not located in the same place in the images. An amplitude error occurs when the two compared plumes are in the same place in the images, but locally their pixels do not have the same values. With the ℒ_{2} pixelwise norm, all the discrepancies are seen as local amplitude errors. This property is illustrated in Fig. 1, where a uniform concentration field 𝒰_{𝔼} is compared to two Gaussian puffs shifted by ϵ=0.054 along the x axis with respect to each other.^{1} The values of the distance are reported in Table 1. In this case, a small position error is penalised by d as much as an absence of plume: this is the socalled double penalty issue. For this metric, the translation cost is composed of two equal contributions. The first is the cost of setting to zero all pixels at the location of the first Gaussian puff. The second is the cost of enhancing the pixels at the translated location.
In the following sections, we further extend the classification of Feyeux et al. (2018) by splitting the amplitude error into two subcategories: the scale error and the shape error. The scale error corresponds to the difference in total amplitude between two shapematching fields, i.e. the difference between the sum of the compared image pixels. The shape error corresponds to the difference between the isocontours after removal of the scale error (i.e. normalisation) and position error (i.e. when both centres of mass and principal axes are superimposed) fields. This splitting of errors is illustrated in the flow chart in Fig. 2.
2.4 Local metric with nonlocal upstream position correction
We propose to address the double penalty issue while still relying on the ℒ_{2} norm by applying an upstream correction of the position error to d. The position error can be seen as a combination of an orientation and a translation error. The orientation error corresponds to the differences that could be reduced by a rotation applied to two concentration fields sharing the same centre of mass location that maximises their overlapping. The translation error corresponds to the difference that could be reduced by a translation applied to two concentration fields.
The new distance is defined in a way that involves finding the rotation and translation that minimise d. The idea is that the rotation should cancel the orientation error, and the translation should cancel the translation error. Let us consider the plane transformation F defined as follows:
which corresponds to a translation of vector ${\mathit{x}}_{t}=({x}_{t},{y}_{t}{)}^{\top}$, followed by a rotation of angle θ and of centre x_{0}+x_{t}, where ${\mathit{x}}_{\mathrm{0}}=({x}_{\mathrm{0}},{y}_{\mathrm{0}}{)}^{\top}$ is the position of the centre of mass of the plume before the transformation. The transformation F depends on three parameters: $({x}_{t},{y}_{t},\mathit{\theta})$. Note that this is an isometry of the plane. The optimal transformation should minimise
However, this cost function is constant for any transformation that moves all the mass of the B plume outside the domain $\mathbb{E}=[\mathrm{0},\mathrm{1}{]}^{\mathrm{2}}$, and by construction X_{B} is then null. This would make the minimisation very difficult with gradientbased optimisation methods. For this reason, we add the following regularisation term to the cost function to penalise any transformation that moves the B plume outside the domain 𝔼:
This regularisation does not affect the location of the minima of d_{F}. The final cost function is
where α is set to the average mass of the A and B plumes, and β is set by trial and error to 10^{4}. In practice, the cost function 𝒥 can be minimised with the limitedmemory Broyden–Fletcher–Goldfarb–Shanno (LBFGS) algorithm (Nocedal and Wright, 2006) that is based on the gradient of 𝒥 with respect to all three parameters θ, x_{t}, and y_{t}, whose expressions are given in Appendix C. To compute the gradient, the spatial partial derivatives of the concentration field X_{B} are needed. Hence, to ensure the continuity of the partial derivatives, we use secondorder bivariate spline interpolation to define the continuous concentration field X_{B} from its original image x_{b}. In order to avoid any issue due to the local nonconvexity of the problem, we also provide a specific initialisation to the minimisation algorithm. The initial translation is then computed using the two centres of mass. Then we do orthogonal regressions to compute the principal axes of both X_{A} and X_{B}. The initial θ is the angle between these axes.
Finally, with the optimal transformation F^{∗}, i.e. the one that minimises 𝒥 defined by Eq. (8), the new distance, called d_{F}, is defined by
For the example of Fig. 1, the values of d_{F} are reported in Table 1 and can be compared to the values of d. In the second case (distance between the two Gaussian puffs), d_{F} is close to zero. The residual value is due to the finite resolution of the images. In the first case (distance between the Gaussian puff and the uniform concentration), d_{F} stays similar to d because any transformation F that keeps the plume in the domain is optimal.
In this section, we introduce the Wasserstein distance, the distance of the optimal transport, as a nonlocal alternative to the pixelwise ℒ_{2} norm.
3.1 Optimal transport and the Wasserstein distance
The optimal transport theory was first introduced in the 17th century by Monge in his famous memoir (Monge, 1781). It is based on the idea that there exists a transport plan to move masses that minimises a given cost of transport. A wider view of the problem was proposed by Kantorovich (1942) using a probabilistic approach. The field has finally regained popularity in the last few decades, in particular with the generalisation by Villani (2009).
In this section, we follow the Kantorovich approach, which means that we will use the discrete representation (see Sect. 2.1). Moreover, the theory is defined only for vectors whose coefficients are nonnegative and sum up to one. While the first condition is satisfied in our case (because we work with images of pollutant concentration), the second is not. Therefore, in the following instead of working with the concentration vectors x_{A} and x_{B}, we will work with their normalised counterparts ${\widehat{\mathit{x}}}_{A}$ and ${\widehat{\mathit{x}}}_{B}$:
where 1∈ℝ^{N} is the vector full of ones and x∈ℝ^{N} is either x_{A} or x_{B}.
The set of couplings P between ${\widehat{\mathit{x}}}_{A}$ and ${\widehat{\mathit{x}}}_{B}$ is defined by
Note that $\mathcal{U}({\widehat{\mathit{x}}}_{A},{\widehat{\mathit{x}}}_{B})$ is not empty because $\mathbf{P}={\widehat{\mathit{x}}}_{A}{\widehat{\mathit{x}}}_{B}^{\top}$ is a coupling between ${\widehat{\mathit{x}}}_{A}$ and ${\widehat{\mathit{x}}}_{B}$. The cost of a coupling $\mathbf{P}\in \mathcal{U}({\widehat{\mathit{x}}}_{A},{\widehat{\mathit{x}}}_{B})$ is defined by
where ${C}_{i,j}\ge \mathrm{0}$ is the (i,j) element of the cost matrix C penalising the transport between ${\widehat{\mathit{x}}}_{A}$ and ${\widehat{\mathit{x}}}_{B}$. Here, it is chosen to be the square of the Euclidean distance between the ith and jth pixels of the original image. For this specific choice, the cost function 𝒥 defined by Eq. (12) has a minimum, which is obtained for a unique coupling P^{∗}. The Wasserstein distance, the distance of the optimal transport, is then defined by
and it is actually a distance according to the mathematical definition. The proofs of these statements can be found in optimal transport textbooks (e.g. Villani, 2009).
Two interesting properties of the Wasserstein distance can be highlighted. First, this metric is defined for normalised vectors only. This means in our case that the difference in total mass between two images is entirely ignored. Alternative solutions have been proposed to take into account this difference, e.g. the one proposed by Farchi et al. (2016) or the use of unbalanced optimal transport (Chizat et al., 2018), but this is beyond the scope of the present study.
Second, following Benamou and Brenier (2000), it is possible to define an optimal transport interpolation between ${\widehat{\mathit{x}}}_{A}$ and ${\widehat{\mathit{x}}}_{B}$. This optimal transport interpolation can help us visualise the idea of vicinity according to w. An example is shown in Fig. 3 for two Gaussian puffs. In the case of the optimal transport interpolation, the w distance between the first puff and the interpolated puff is linearly growing (by the construction of the interpolation), while the increase of the d distance is at first very steep. In some sense, this behaviour was expected since the first puff and the interpolated puff are quickly separated from each other. In the case of the linear interpolation, the same phenomenon happens: the d distance is linearly growing (by the construction of the interpolation), while the increase of the w is steeper, but not as steep as the increase of d in the first case. This shows that the Wasserstein distance w is a metric that better handles the position error than d, since it accounts linearly for the mismatch in the plume positions.
3.2 Sinkhorn's algorithm
To compute the Wasserstein distance, we have to determine the optimal coupling matrix P^{∗} by minimising 𝒥 defined by Eq. (12). The convexity of the cost function 𝒥 is not guaranteed; thus it is usual (see, e.g. Peyré and Cuturi, 2019, and references therein) to add the following entropic regularisation:
The objective function to minimise becomes
under the same constraint $\mathbf{P}\in \mathcal{U}\left({\widehat{\mathit{x}}}_{A},{\widehat{\mathit{x}}}_{B}\right)$. The solution of the regularised problem is an approximation of the Wasserstein distance. When ϵ→0, it converges toward the exact value of the Wasserstein distance $w\left({\widehat{\mathit{x}}}_{A},{\widehat{\mathit{x}}}_{B}\right)$; when ϵ→∞, the optimal coupling matrix converges toward $\mathbf{P}={\widehat{\mathit{x}}}_{A}{\widehat{\mathit{x}}}_{B}^{\top}$.
It is possible to show that minimising Eq. (15) is equivalent to minimising the Kullback–Leibler divergence between $\mathbf{P}\in \mathcal{U}\left({\widehat{\mathit{x}}}_{A},{\widehat{\mathit{x}}}_{B}\right)$ and the Gibbs kernel $\mathbf{K}=\mathrm{exp}\left(\mathbf{C}/\mathit{\u03f5}\right)$, where the exponential is applied entrywise, which is given by
The advantage of this formulation it that this problem is known to admit a unique solution which is the projection of the Gibbs kernel K onto $\mathcal{U}({\widehat{\mathit{x}}}_{A},{\widehat{\mathit{x}}}_{B})$. This unique solution can be written
where u and v are vectors with positive or null entries satisfying
In these equations, ∘ is the Schur–Hadamard (i.e. entrywise) product in ℝ^{N}.
The (u,v) factorisation is unique and can be easily found using the iterative update scheme proposed by Sinkhorn, where the lth update is given by
where ÷ is the entrywise division in ℝ^{N}.
3.3 Logformulation of Sinkhorn's algorithm
Sinkhorn's algorithm provides a simple and quick solution to the optimal transport problem. However, this formulation raises technical issues. The first is that for small values of ϵ – which is what we are aiming for to be as close as possible to the true optimal transport solution – the algorithm converges slowly.^{2} To accelerate the convergence, we use a high value of ϵ and progressively decrease it whenever (u,v) has converged. We will use this technique in our experiments.
Another numerical issue appears when ϵ is small compared to the entries of C. In this case, u, v, and K explode and cannot be computed with finite numerical precision. To address this issue, we adopt the logSinkhorn algorithm proposed by Peyré and Cuturi (2019), which is presented in the following lines.
Let us introduce f and g, which are related to u and v by
Instead of updating (u,v) with Sinkhorn iteration Eq. (19), we update (f,g) using
Combining the logSinkhorn algorithm while decreasing ϵ is not straightforward, because there are a lot of numerical decisions to make: intermediate and final values of ϵ, convergence criteria, etc. After several tests, we ended up with Appendix A, which we found to be a good tradeoff between speed and accuracy. The value of ϵ is progressively decreased from 1 to 10^{−5}: each time the convergence criterion is met, ϵ is reduced by a factor of 10. In our case, the convergence criterion is met when the relative difference between the former and the current value of the Wasserstein distance falls below $\mathit{\zeta}=\mathrm{5}\times {\mathrm{10}}^{\mathrm{4}}$. In addition, we set a maximum number of Sinkhorn iterations of 200 per value of ϵ to keep the computational cost under control. Finally, note that, for a given ϵ, one can try to accelerate the convergence by using the averaging step proposed in Chizat et al. (2018), but this is beyond the scope of the present study.
3.4 Gaussian approximation and upstream correction
Following the derivation of Sect. 2.4, we want to apply the same upstream correction of the position error to the Wasserstein distance w. However, this would require the gradient of the Wasserstein distance w with respect to each one of its inputs. The computation is not straightforward, even taking into account the logSinkhorn formulation developed in Sect. 3.3. For this reason, we will use the Gaussian approximation, for which the Wasserstein distance has an analytical formula.
More specifically, we assume that we have two continuous concentration fields X_{A} and X_{B} that follow the Gaussian puff model:
with Σ_{A} and Σ_{B} given by
In this case, the squared Wasserstein distance between X_{A} and X_{B} is given by^{3}
Following the approach of Sect. 2.4, let us now apply the plane transformation F given by Eq. (5) to X_{B}. The squared Wasserstein distance becomes
which depends on x_{t}, y_{t}, and θ, the three parameters of F. It can be shown (see Appendix D) that ${w}^{\mathrm{2}}({X}_{A},{X}_{B}\circ \mathbf{F})$ reaches its minimum when ${\mathit{x}}_{t}={\mathit{\mu}}_{A}{\mathit{\mu}}_{B}$ and $\mathit{\theta}={\mathit{\theta}}_{A}{\mathit{\theta}}_{B}$ (modulo π), in which case the distance is given by
which is known as the Hellinger distance between X_{A} and X_{B} (Peyré and Cuturi, 2019). By construction, this distance estimates the shape error between X_{A} and X_{B}, since the translation, the rotation, and the scale differences have been removed. In the following, it will be written w_{F} to point out the similarity between the relationship $d/{d}_{F}$ on the one hand and $w/{w}_{F}$ on the other hand. In the case where X_{A} and X_{B} are not exactly Gaussian, we can still use the Gaussian puff model as an approximation. In this case, w_{F} provides an approximation of the shape error.
Finally, an issue with both w and w_{F} is that they are normalised fields, and thus they ignore the scale error, i.e. the difference of total mass between the images. As a consequence, these metrics cannot be used as such in an inversion framework. One way to address this issue is to add to w and w_{F} a term to represent the scale error. Using discrete formalism, this term could be
which is convex. The remaining question would then be the relative contribution of w (or w_{F}) and d_{mass} in the final distance, which is related to the following question: which kind of error (position, mass, etc.) should be penalised more? This kind of question is beyond the scope of the present article, which is why we only use w and w_{F} as is in our numerical experiments.
In this section, we evaluate and compare the metrics with a database of images built using a set of Gaussian puffs. The database is introduced in Sect. 4.1, the computation of the nonlocal metrics is validated in Sect. 4.2, and the behaviour of the metrics on this Gaussian puff database are compared in Sect. 4.3.
4.1 Gaussian puff database and experimental setup
The database consists of 10^{4} pairs of images constructed using Gaussian puffs and then discretised on the domain $\mathbb{E}=[\mathrm{0},\mathrm{1}{]}^{\mathrm{2}}$ using a finite resolution of 32×32 pixels. Each puff is parameterised by its mean μ (two scalars) and its covariance matrix $\mathbf{\Sigma}=\mathbf{R}\left(\mathit{\theta}\right)\mathbf{\Delta}\mathbf{R}(\mathit{\theta}{)}^{\top}$ (three scalars: θ and both diagonal entries of Δ), which are randomly drawn as follows:

Both components of μ are uniformly drawn in [0.15,0.85].

θ is uniformly drawn in $[\mathit{\pi},\mathit{\pi}]$.

σ_{1} and then σ_{2}, the two nonzero components of Δ, are drawn from a halfnormal distribution with a standard deviation of 0.33. If needed, σ_{1} and σ_{2} are then swapped to ensure σ_{1}≥σ_{2}.
Ideally, the domain 𝔼 should cover a large majority of the mass of each puff. In practice, more than 99 % of the mass of a Gaussian puff is covered by the 6σ_{1}×6σ_{2} rectangle centred on μ and oriented along the principal axes. For this reason, we repeat step 3 of the random draw until this 6σ_{1}×6σ_{2} rectangle is included in the domain 𝔼. In addition, the puffs should not be too small, which is why in our case when 6σ_{1} and 6σ_{2} are both smaller than 9 pixels, it is rejected and entirely redrawn.
The characteristics of the database are shown in Fig. 4 and cover the analytical pathological situations described in Davis et al. (2009). As expected, the distribution of $\Vert \mathit{\mu}\Vert $ is close to Gaussian, the distribution of θ is close to uniform, and the distribution of σ_{1} and then σ_{2} are close to lognormal.
4.2 Validation of the implemented Sinkhorn algorithm
For our Gaussian puff database, there are four different ways to compute the Wasserstein distance:

The analytical formula Eq. (24) can be used with the exact values of μ_{A,B} and Σ_{A,B}. This approach will be called w_{th}.

The analytical formula Eq. (24) can be used but with μ_{A,B} and Σ_{A,B} being the sample mean and covariance of the 32×32pixel images. This approach is closer to what will be practically done for real image plume, extracting information only from the image, and it will be called w_{num}.

The network simplex algorithm (Bonneel et al., 2011) can be used to find the exact solution of the optimal transport problem using the images like w_{num}. This approach will be called w_{emd}.

The logSinkhorn iterations can be applied using Appendix A using the images like w_{num}. This approach will be called w_{ϵ}.
We have applied all four methods, and the differences are shown in Fig. 5. Note that w_{emd} has been computed using the Python Optimal Transport (POT) library (Flamary et al., 2021).
The fractional bias over all pairs is no more than 5 % when we compare w_{th} to the other three methods of computing the Wasserstein distance. By contrast, w_{emd} and w_{num} are very close to each other. We have checked that the latter phenomenon is reduced when the resolution is increased. Therefore, we conclude that the gap between w_{th} on the one hand and w_{num}, w_{emd}, and w_{ϵ} on the other hand is not due to the estimation of the Wasserstein distance but results from the discretisation of the problem with the 32×32 resolution (sampling errors). Figure 5 also shows that w_{ϵ} matches w_{emd} well, which validates our logSinkhorn implementation.
4.3 Correlation to the different error categories
In this subsection, we compare the behaviour of the metrics with respect to three error categories: the translation error, the orientation error, and the shape error. Note that the behaviour with respect to the scale error cannot be compared since the w and w_{F} distances use normalised images. We used the Pearson correlation as our main indicator of the strength of the link between the behaviour of the metrics and the error category. The closer the norm of the Pearson correlation is to 1, the more linear the relation between the quantities is. If the Pearson correlation is positive, then the increase in an error category leads to an increase in the metric value, if negative it leads to a decrease, and if nearly null it means that the two quantities seem independent.
For each pair of images in the database, we define T (for translation) as $\Vert {\mathit{\mu}}_{B}{\mathit{\mu}}_{A}{\Vert}^{\mathrm{2}}$. This quantity represents the translation error between both images. The correlation between T and the four distances is reported in the first column of Table 2.
As expected, the Wasserstein distance w is strongly correlated to T. The ℒ_{2} norm d is also showing a significant correlation of 0.33 to T, highlighting a likely dependency. Both d_{F} and w_{F} are designed to be released from the position error and, in particular, the translation error. This property is confirmed by the very low correlation between T on the one hand and d_{F} and w_{F} on the other hand. Additionally, the fact that T is much more correlated to d than to d_{F} confirms that d indeed depends on the T quantity.
For each pair of images in the database, we define θ as $\Vert {\mathit{\theta}}_{B}{\mathit{\theta}}_{A}\Vert $. This quantity represents the orientation error between both images. The correlation between θ and the four distances is reported in the second column of Table 2. The results show also that there is no correlation between θ and any of the distances. In a sense, this shows that all the distances are, for our database, not sensitive to the orientation error.
For each pair of images in the database, we define H as the Hellinger distance between A and B, as given by Eq. (26). This is actually very similar to w_{F}, but with one exception: H uses the theoretical values of Δ_{A} and Δ_{B} (i.e. the ones that have been drawn), while w_{F} uses the sample covariance of the 32×32pixel images. This quantity represents the shape error between both images. The correlation between H and the four distances is reported in the third column of Table 2.
Both d and w show a low correlation to H, which is not the case of d_{F} and w_{F}. On the one hand, the correlation between w_{F} and H was highly expected from the definition of H. The remaining difference is due to the finite resolution of the images. On the other hand, the proportionality of d_{F} with the H was wanted but not assessed. By superimposing optimally the plumes, we removed the position error, but d_{F} remains sensitive to H, meaning we did not remove all errors. Thus such behaviour reflects our way of splitting the error. More generally, this comparison on the Gaussian puff database confirms that both d_{F} and w_{F} are freed from the position error and seem to be driven by the shape error.
To go deeper in our analysis, we now compare the metrics using realistic plumes. This section follows the same organisation as Sect. 4: we present the experimental setup in Sect. 5.1, we validate the computation of the nonlocal metrics in Sect. 5.2, and we compare the behaviour of the metrics on this specific database in Sect. 5.3.
5.1 Simulation database and experimental setup
We use a simulation database of hourly 3D fields of CO_{2} concentrations due to anthropogenic CO_{2} emissions from the Neurath lignitefired power plant (Germany, 51.04^{∘} N, 6.60^{∘} E). The database is extracted from a larger one, over western Europe, as described in Potier et al. (2022). Simulations were performed with the CHIMERE Eulerian transport model (Menut et al., 2013) driven by the Community Inversion Framework (CIF; Berchet et al., 2021). The resolution of the simulation (longitude: 6.82^{∘} W to 19.18^{∘} N; latitude: 42.0 to 56.39^{∘} N, Fig. 6; Santaren et al., 2021) goes from 50 to 2 km. The Neurath power plant is located in the 2 km × 2 km resolution zoom (longitude: 1.25^{∘} W to 10.64^{∘} E; latitude: 47.45 to 53.15^{∘} N). The vertical grid is composed of 29 pressure layers extending from the surface to 300 hPa (approximately 9 km above the ground level). CHIMERE is forced by meteorological variables at 9 km resolution (AgustiPanareda, 2018), provided by the European Centre for MediumRange Weather Forecasts (ECMWF) for the CO_{2} Human Emissions project (CHE; https://www.cheproject.eu/, last access: 14 March 2023). The CO_{2} emissions from the Neurath power plant are extracted from the ∼ 1 km ($\mathrm{1}/\mathrm{60}$^{∘} × $\mathrm{1}/\mathrm{120}$^{∘}) resolution inventory (TNO_GHGco_1x1km_v1_1) of the annual emissions produced by the Netherlands Organisation for Applied Scientific Research (TNO) over Europe for the year 2015 (Denier van der Gon et al., 2017; Super et al., 2020). The temporal disaggregation at the hourly scale is based on coefficients provided with the TNO inventories for the sector APublic Power, in the Gridded Nomenclature For Reporting (GNFR) of the United Nations Framework Convention on Climate Change (UNFCCC). Emissions are projected on the CHIMERE vertical grid with coefficients corresponding to this A GNFR sector (Bieser et al., 2011), also provided with the TNO inventories. We simulate 14 d of 1 h emission pulses at the Neurath power plant location, from 1 to 14 July 2015, i.e. 336 puffs. The transport of these puffs is simulated until midnight. Consequently, the later in the day the puffs are emitted, the shorter they are tracked. Assuming that the source continuously releases CO_{2}, the puffs are aggregated to create plume images for every hour. Due to this experimental setup, the plume follows a 24 h cycle. It appears after 0 h and grows until past 24 h of simulation and then restarts.
We ensure that the daily evolution of the hourly emission rate from the source is the same for all plumes. Hence, for a given hour of the day, the difference between two simulated plumes from two different days is due to the meteorology. We build a database that regroups per pair simulated plumes at a given hour but from different days (e.g. day 1 hour 10 versus day 3 hour 10). To get a realistic twodimensional concentration field, we compute the vertical mean of the concentration weighted by the width of the vertical levels. We ignore the first 2 h of the simulation, to ensure that a plume appears in the image. This leaves 2093 pairs of distinct plumes. The images are cropped to 100 × 100pixel (here 1 pixel is equal to 2 km square cell of the simulation) images to reduce the computer resource requirements.
5.2 Comparison of the different estimations of the Wasserstein distance
We have applied all three methods, and the differences are shown in Fig. 7. The results show, as for the Gaussian puff database, that w_{ϵ} and w_{emd} are close to each other, which once again validates our algorithm. Moreover, the results show that w_{num} is a reasonably good approximation of w as well. The distance w_{num} makes the approximation that the images are Gaussian puffs, which is a strong approximation but allows for very quick computation. The values of w_{num} seem to be usually lower than those of w_{ϵ}. This previous remark is in agreement with Theorem 2.1 from Gelbrich (1990). It is shown that, for elliptic contour distributions with given mean and covariance matrices, the distance between the two Gaussians with these respective parameters (i.e. w_{num}) is a lower bound of the Wasserstein distance between the two distributions. We are not assured to work with plumes that are elliptic distributions. However, it seems to be a good direction to look at to explain and quantify, if possible, this negative bias. The understanding of the discrepancies between w_{num} and w_{ϵ} is needed to be able to substitute w_{num} to w_{ϵ}. For this reason, w_{num} is not tested further in the following sections.
5.3 Correlation to the different error categories
In this subsection, we compare the behaviour of the metrics with respect to the same three error categories as in Sect. 4.3: the translation, orientation, and shape error. To do so, we keep the same quantities T, θ, and H, with the notable exception that H is now equal to w_{F} because there is no theoretical covariance. The results are reported in Table 3.
While the correlation between w and T remains very strong, d shows less correlation to T than for the Gaussian puff database. Both d_{F} and w_{F} are less correlated to T than d and w, respectively, but their correlation to T is here higher than with the Gaussian puff database. Hence for this realistic database, both d_{F} and w_{F} are only partially freed from the translation error.
In this case, the correlations between the metrics and θ are higher than for the Gaussian puff database but again do not prompt a clear conclusion.
By construction, w_{F} is equal to H, which yields a correlation of 1. Both d and w show a small correlation to H, which was not the case in the Gaussian puff database. The correlation to H is still higher for d_{F}, which was expected since d_{F} is designed to be partially freed from the position error. This result, however, should be taken with caution because here, contrary to the Gaussian puff database, H now only partially accounts for the shape error between two plumes.
This second study with realistic cases shows that the behaviour of each metric slightly differs from what has been seen in the Gaussian case. Nevertheless, the results confirm that both d_{F} and w_{F} are partially freed from the position error while being still sensitive to the shape error, which is what we hoped for.
As stated in the introduction, the goal of this article is to develop and test metrics that can discriminate errors stemming from imperfect meteorology from other sources of discrepancies. Therefore, following the approach used in the previous sections, we define here four indicators that we consider representative of the difference in meteorological conditions between the two images. We then examine the correlation between these indicators, the previous indicators (T, θ, and H), and the metrics in the case of the realistic database.
6.1 Definition of meteorological indicators
To simplify the analysis, we define four scalar indicators that characterise the meteorological conditions. These indicators focus on the direction and the norm of the wind as experienced by the pollutant during its transportation. For each image, we proceed as follows.

We first average the wind components (threedimensional fields) in the vertical direction between the surface and the planetary boundary layer (PBL) height. Indeed, the realistic database has been simulated with summer conditions, and hence the plumes are assumed to be dispersed within the PBL. This results in twodimensional fields for each time snapshot.

We compute the norm and the direction of the averaged winds. This results in two twodimensional fields for each time snapshot.

We average the norm and the direction over the 100×100pixel grid. This results in two scalars for each time snapshot.

We finally compute the time average and time standard deviation of the averaged norm and direction between midnight (the time at which the emissions started) and the time of the image. This results in four scalars: E_{N} (averaged wind norm), E_{D} (averaged wind direction), S_{N} (deviation of wind norm), and S_{D} (deviation of wind direction).
The meteorological indicators are then defined as the absolute differences in E_{N}, E_{D}, S_{N}, and S_{D} between the two images that are compared, simply written ΔE_{N}, ΔE_{D}, ΔS_{N}, and ΔS_{D}.
6.2 Correlation between the meteorological indicators and the error categories
Using the realistic database, we compute the correlation between ΔE_{N}, ΔE_{D}, ΔS_{N}, and ΔS_{D} on the one hand and T, θ, and H on the other hand. The idea is to see how differences in the meteorological conditions impact the position and amplitude errors. The results are reported in Table 4.
One can notice that T is mainly correlated to ΔE_{D} and a little less to ΔE_{N}, while ΔS_{D} and ΔE_{D} are correlated to H. This means that differences in meteorology like ΔE_{D} will likely induce both position error and shape error. Therefore, by removing the position error, we only partially remove the meteorological impact on the differences. Explaining why ΔS_{D} induces differences in shape is straightforward, but explaining how ΔE_{D} induces differences in terms of translation instead of orientation is not as so. A difference in the main direction of the plume (which translates into ΔE_{D}) will move further away the centres of mass from each other and hence induce a larger T (which is the distance between the two centres of mass). It should be noted that a wind direction change that will keep superimposed the centre of mass will drive orientation error.
6.3 Correlation between the meteorological indicators and the metrics
To conclude our study, we now compare the different metrics to the meteorological indicators. The results are reported in Table 5.
According to the correlations shown in Table 5, the metric w is correlated to ΔE_{D} and ΔE_{N} indicators. This is expected since these meteorological changes tend to move the centre of mass and thus increase the translation error. The results show also that w_{F} sees a drop in correlation to ΔE_{D} compared to w while getting a correlation with respect to ΔS_{D}. For optimal transport metrics, we can see that removing the position error does not always remove the sensitivity to a change in meteorology. It should be noticed that increasing in either d or d_{F} does not seem to be more correlated to our different meteorology indicators. Such a lack of correlation compared to the optimal transport theory metrics could result from the weight of the scale error in the distance definition. We normalised the plume the same way as we do for w before computing the distance d and d_{F}, leading us to the normalised image distances d^{∗} and ${d}_{F}^{\ast}$. First, d^{∗} and ${d}_{F}^{\ast}$ are more correlated than d and d_{F} to ΔE_{D} and ΔS_{N}, showing that the scale error is masking the sensitivity of pixelwise metrics with respect to meteorology. Second, ${d}_{F}^{\ast}$ gains significantly in correlation to ΔS_{D} compared to d^{∗} but remains as correlated to ΔE_{D} as d^{∗}. Then the plane transformation applied in ${d}_{F}^{\ast}$ allows a better alignment of the compared plumes, giving more weight to shape error induced by ΔS_{D}, but does not compensate for all the changes resulting from ΔE_{D} or ΔE_{N}.
The lack of correlation to our meteorological indicators for d and d_{F} seems appealing, but it is due to amplitude error held by a small number of highly concentrated pixels above the source for our cases (i.e. a hotspot). For similar cases, d remains a good metric for updating the inventories. If the “hotspots” of the two images have amplitudes close to each other or there is no “hotspot” but a large plume, d and d_{F} become more correlated to several meteorological changes, making them less suitable. Pixelwise metrics seem to be better adapted to compare “hotspot” and not highly extended plumes. A more versatile metric will be a weighted distance using the w_{F}, or at least a normalised ${d}_{F}^{\ast}$, which is not sensitive to all changes in meteorology, and a term that represents the scale error between the two images.
In this article, we discussed the use of new metrics for comparing passive gas plumes, practically CO_{2} plumes, within an inverse framework aiming at the monitoring of pollutant emissions.
At first, we emphasised how critical the double penalty issue related to pixelwise comparison is. The traditional ℒ_{2} norm tends to overweight position errors mixing up with other sources of errors. In the context of source inversion, this results in an overpenalised comparison of concentration fields that are slightly shifted from each other, and the mixing makes it difficult to evaluate the relative weight of different types of error afterwards. Yet, for us, the identification of the relative weight of the errors is critical, since we want to level down the one due to meteorology and level up the one related to emissions. Assuming that most of the position error is driven by meteorology, we proposed to design metrics that are freed from position error. Following this goal, a pixelwise metric with an upstream position correction was designed. This new metric has the advantage of keeping the formalism of the ℒ_{2} norm while being released from position errors. In addition, it is proposed to use a metric based on the optimal transport theory: the Wasserstein distance. Focusing on the algorithmic aspects related to twodimensional satellite images, we derived and validated a method to compute this metric. The Wasserstein metric is more sensitive to position errors, but it is not hampered by the double penalty issue. To complete our catalogue of metrics, an optimal transport metric freed from position errors is proposed. It can be easily computed with a Gaussian approximation. This metric coincides with the Hellinger distance. Nevertheless, both optimal transport metrics rely on normalised images and thus are unaware of the difference in the total mass present in the plumes. The scale factor between the images is linearly related to emission fluxes which we want to estimate. This means that, within the inversion framework, the scale factor between the two images should be added and weighted independently.
These four metrics were compared on a specifically designed Gaussian puff database and evaluated according to their correlations with respect to translation error, orientation error, and shape error. The numerical experiments showed that the resolution of the images tends to impact the optimal transport problem. As expected, the two metrics designed to be freed from position errors are not correlated to translation and orientation errors. The ℒ_{2} norm and Wasserstein metrics are both correlated to the translation error. From this, we extended our tests to a realistic plume database. This second test series shows that, for a more complex plume geometry, the metrics are still correlated to the translation error. This implies that the new metrics are only partially freed from position errors.
Then we discussed the link between a position error and a variation within the mesoscale meteorology using the same realistic database. Designing relevant scalar indicators related to meteorological variance, we evaluated how specific changes in meteorological conditions lead to an increase in the distance between the plumes. We have seen that the meteorological changes can be correlated to position errors as well as amplitude errors between plumes. This means that removing the position error from the metrics will not make the comparison insensitive to a meteorological change. However, some metrics were found to be more sensitive to specific changes in meteorological conditions. For instance, while the Wasserstein metric is sensitive to changes in the main direction or intensity of the winds, the Hellinger metric is more sensitive to changes in the spread of the wind direction both in time and space. This provides guidelines to enlighten the choice of a metric for a given meteorological situation. By composing this with these new metrics freed from position error and additional scaling terms, we get more manageable metrics that will level down in the weight of modelling error due to the meteorology used in the comparison.
These metrics are used to quantify the proximity of a couple of plumes and could hence be used in an inverse framework, in particular for processing XCO_{2} images. The question of the impact of the meteorological changes on the metrics discussed here can be translated into another question: what importance do we give to each error category? We know that meteorological changes can result in position errors, and we strongly suspect that changes in the emission's temporal profile or vertical distribution can also yield position errors. In such a case, it would be interesting to evaluate the impact of the removal of the position errors and whether the amplitude errors carry enough information to compensate. We have seen that amplitude errors can also emerge from changes in meteorology. Thus further studies have to be undergone to evaluate the sensitivity of the metrics to either the emissions or the meteorology, to determine which error has to be more weighted from the perspective of monitoring the emissions. We have to make sure that by removing some sensitivity with respect to meteorology, we are not levelling down by the same factor the sensitivity with respect to the emissions.
For an operational purpose, optimising on nonlocal metrics is much more difficult than on pixelwise metrics because it requires the computation of nontrivial gradients. The three nonlocal metrics that we proposed are parameterised. These parameters usually balance a tradeoff between computational efficiency and accuracy. In the case of the pixelwise distance with an upstream correction, the choice of the optimal isometry to apply depends on these parameters. Even though this study could be done with a personal computer, further computation optimisation developments are needed for operational use. Here we are only considering passive tracers, but an extension of the study should be using these metrics for reactive pollutants. However, it requires quantifying the relative impact of chemistry on the shape, scale, and position of the plume.
The key idea here is that meteorology is fixed and bounds our model predictions. We choose to develop metrics that aim to remove the weight of such bound within the comparison to the observation. We could instead consider that meteorology is not fixed and can be seen as additional degrees of freedom to estimate. Thus the Wasserstein metric is interesting because it penalises the position error linearly, but it remains numerically costly compared to pixelwise metrics. Yet, we have seen that approximating the plume by Gaussian puffs yields a cheap estimate of the true Wasserstein distance. To ease the computation, we suggest using an approximation of the Wasserstein distance, assuming Gaussian pufflike plumes or separable into a Gaussian mixture as in Chen et al. (2019) and Delon and Desolneux (2020). But the relevance of these approximations has to be discussed when it comes to real, noisy, cloudy, plume images. This paper was a first step towards the use of smarter metrics to compare plume images to monitor atmospheric gaseous compound emissions through an inverse method.
x  Position vector in the image 
X_{A,B}  Continuous interpolation of the concentration field 
x_{A,B}  Discrete representation of the concentration field 
${\widehat{\mathit{x}}}_{A,B}$  Normalised discrete concentration field 
𝒩(μ,Σ)  Normal distribution of mean μ and error covariance matrix Σ 
𝒰_{𝔼}  Uniform distribution over the domain 𝔼 
μ  Always refers to a mean vector 
Σ  Always refers to an error covariance matrix 
Δ  Diagonal matrix with the eigenvalues of Σ 
R(θ)  Rotation matrix of angle θ 
x_{t}  Translation vector 
x_{0}  Centre of mass coordinate vector 
F  Transformation in the plane 
d  Usual pixelwise Euclidean distance 
d_{F}  Pixelwise distance with an upstream position correction 
w  Wasserstein distance 
w_{F}  Wasserstein distance with an upstream position correction 
w_{emd}  Earth mover distance 
w_{ϵ}  LogSinkhorn approximation of the Wasserstein distance 
w_{num}  Wasserstein distance between two Gaussian puffs 
w_{th}  Analytical Wasserstein distance between two Gaussian puffs 
ϵ  Weight of the entropic regularisation of the logSinkhorn algorithm 
ζ  Convergence criterion for the logSinkhorn algorithm 
T  Translation length between the centre of mass of two plumes 
θ  Rotation angle between the principal axes of two plumes 
H  Hellinger distance between the error covariance matrices of two plumes 
E_{N}  Mean wind speed seen by the plume averaged over the image domain and time 
E_{D}  Mean wind direction seen by the plume averaged over the image domain and time 
S_{N}  Standard deviation of the wind speed seen by the plume across the image domain and time 
S_{D}  Standard deviation of the wind direction seen by the plume across the image domain and time 
To minimise Eq. (8) we use the LBFGS algorithm provided by the SciPy library. The algorithm explicitly uses the gradient of the cost function 𝒥 with respect to θ, x_{t}, and y_{t}. The first term of this gradient – corresponding to ${d}^{\mathrm{2}}\left({X}_{A},{X}_{B}\circ \mathbf{F}\right)$ – is given by
where α is either θ, x_{t}, or y_{t}, $\mathit{x}={\left(x,y\right)}^{\top}$, and $\mathbf{F}={\left({F}_{x},{F}_{y}\right)}^{\top}$. The partial derivatives of X_{B} are given by the second image (using the interpolation method), and the partial derivatives of F_{x} and F_{y} are
Let us define the cost function
where ${w}^{\mathrm{2}}\left({X}_{A},{X}_{B}\circ \mathbf{F}\right)$ is given by Eq. (25). The goal is to minimise 𝒥. From Eq. (25), we remark that 𝒥 has three terms $\mathcal{J}={\mathcal{J}}_{\mathrm{1}}+{\mathcal{J}}_{\mathrm{2}}+{\mathcal{J}}_{\mathrm{3}}$, with
Minimising 𝒥 with respect to $\left({x}_{t},{y}_{t},\mathit{\theta}\right)$ is equivalent to minimising 𝒥_{2} with respect to (x_{t},y_{t}) and minimising 𝒥_{3} with respect to θ. The minimum of 𝒥_{2} is 0 and is reached for ${\mathit{x}}_{t}={\mathit{\mu}}_{B}{\mathit{\mu}}_{A}$. Let us now focus on the minimum of 𝒥_{3}. For convenience, we define
in such a way that ${\mathcal{J}}_{\mathrm{3}}\left(\mathit{\theta}\right)=\mathrm{2}\mathrm{Tr}\mathbf{M}{\left(\mathit{\theta}\right)}^{\frac{\mathrm{1}}{\mathrm{2}}}$. With our notation, we have
where $\stackrel{\mathrm{\u0303}}{\mathit{\theta}}\triangleq \mathit{\theta}+{\mathit{\theta}}_{B}{\mathit{\theta}}_{A}$, and hence
By construction, M(θ) is symmetric and positive definite; therefore it is diagonalisable with strictly positive eigenvalues λ_{±}(θ). As a consequence, we have
Let us now introduce the following ancillary quantities:
Note that γ(θ) is the discriminant of the characteristic polynomial of M(θ), which means that γ(θ)≥0 because M(θ) is symmetric and positive definite. With these quantities, we have
Let us first consider the case γ(θ)=0. In this case, ${\mathit{\lambda}}_{+}\left(\mathit{\theta}\right)={\mathit{\lambda}}_{}\left(\mathit{\theta}\right)\triangleq \mathit{\lambda}\left(\mathit{\theta}\right)$; in other words M(θ)=λ(θ)I. From the definition of M(θ), Eq. (D5), we deduce that
which enforces $\stackrel{\mathrm{\u0303}}{\mathit{\theta}}=\mathrm{0}$ (modulo π). This means that Eq. (D7) simplifies into
and hence $\mathit{\lambda}\left(\mathit{\theta}\right)={\mathit{\sigma}}_{\mathrm{1},A}{\mathit{\sigma}}_{\mathrm{1},B}={\mathit{\sigma}}_{\mathrm{2},A}{\mathit{\sigma}}_{\mathrm{2},B}$. Without loss of generality, we can assume in the definition of Δ_{A} and θ_{A} that $\mathrm{0}<{\mathit{\sigma}}_{\mathrm{1},A}\le {\mathit{\sigma}}_{\mathrm{2},A}$ and the same for B.^{4} This means that ${\mathit{\sigma}}_{\mathrm{1},A}{\mathit{\sigma}}_{\mathrm{1},B}={\mathit{\sigma}}_{\mathrm{2},A}{\mathit{\sigma}}_{\mathrm{2},B}$ actually implies ${\mathit{\sigma}}_{\mathrm{1},A}={\mathit{\sigma}}_{\mathrm{2},A}$ and ${\mathit{\sigma}}_{\mathrm{1},B}={\mathit{\sigma}}_{\mathrm{2},B}$. In this case, the covariance matrices for A and B are isotropic, and 𝒥_{3} does not actually depend on θ.
Let us now consider the nonisotropic case: $\mathrm{0}<{\mathit{\sigma}}_{\mathrm{1},A}<{\mathit{\sigma}}_{\mathrm{2},A}$ and $\mathrm{0}<{\mathit{\sigma}}_{\mathrm{1},B}<{\mathit{\sigma}}_{\mathrm{2},B}$, which is the only case where 𝒥_{3} depends on θ. In this case, we necessarily have γ(θ)>0. We can then take the derivative of 𝒥_{3} with respect to θ:
which is the product of three terms: β−α, $\mathrm{cos}\stackrel{\mathrm{\u0303}}{\mathit{\theta}}\mathrm{sin}\stackrel{\mathrm{\u0303}}{\mathit{\theta}}$, and $\left(\sqrt{{\mathit{\lambda}}_{+}\left(\mathit{\theta}\right)}\sqrt{{\mathit{\lambda}}_{}\left(\mathit{\theta}\right)}\right)/\sqrt{\mathit{\gamma}\left(\mathit{\theta}\right)}$. The third term is always strictly positive because γ(θ)>0. The first term is always strictly negative because we have assumed that ${\mathit{\sigma}}_{\mathrm{1},A}<{\mathit{\sigma}}_{\mathrm{2},A}$ and ${\mathit{\sigma}}_{\mathrm{1},B}<{\mathit{\sigma}}_{\mathrm{2},B}$. Hence we only need to consider the second term $\mathrm{cos}\stackrel{\mathrm{\u0303}}{\mathit{\theta}}\mathrm{sin}\stackrel{\mathrm{\u0303}}{\mathit{\theta}}$ to conclude that the minima of 𝒥_{3} are met for $\stackrel{\mathrm{\u0303}}{\mathit{\theta}}=\mathrm{0}$ (modulo π) or equivalently $\mathit{\theta}={\mathit{\theta}}_{A}{\mathit{\theta}}_{B}$ (modulo π). In this case, M(θ)=Δ_{A}Δ_{B} and ${\mathcal{J}}_{\mathrm{3}}\left(\mathit{\theta}\right)=\mathrm{2}\mathrm{Tr}\left({\mathbf{\Delta}}_{A}{\mathbf{\Delta}}_{B}\right)$, which yields the correct formula for w_{F}, Eq. (26). Finally, note that this formula is also valid in the case where at least one of A or B is isotropic.
All the data required to get the presented results are available in the Zenodo repository (https://doi.org/10.5281/zenodo.6958047, Vanderbecken, 2022). All the graphics utilize scientific colour maps developed by Crameri (2021) and are available at https://doi.org/10.5281/zenodo.5501399.
Writing process: mainly PJV and EP with inputs from all coauthors. System and experiment design: PJV, JDLB, AF, MB, and YR. Implementation: PJV. Support in development and use of data: PJV and EP. Analysis: mainly PJV, JDLB, AF, and MB, with feedback from YR, EP and GB.
The contact author has declared that none of the authors has any competing interests.
Publisher’s note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
This study has been funded by the national research project ANRARGONAUT no. ANR19CE010007 (PollutAnts and gReenhouse Gases emissiOns moNitoring from spAce at high ResolUTion). Joffrey Dumont Le Brazidec is supported by the European Union's Horizon 2020 research and innovation programme under grant agreement no. 958927 (Prototype system for a Copernicus CO2service). All the figures were drawn using CVDfriendly colour maps. This was made possible using a Python wrapper around Fabio Crameri's perceptually uniform colour maps (Crameri, 2021), available here: https://www.fabiocrameri.ch/colourmaps/ (last access: 14 March 2023). CEREA is a member of Institut PierreSimon Laplace (IPSL). The authors jointly thank the associate editor, Lok Lamsal, and the two anonymous referees for the relevant comments they made during the review of this article.
This research has been supported by the national research project ANRARGONAUT (grant no. ANR19CE010007, PollutAnt and gReenhouse Gases emissiOns moNitoring from spAce at high ResolUTion).
This paper was edited by Lok Lamsal and reviewed by two anonymous referees.
AgustiPanareda, A.: The CHE Tier1 Global Nature Run, Tech. rep., CO_{2} Human Emissions, H2020 European Project, https://www.cheproject.eu/sites/default/files/201807/CHED2.2V10.pdf (last access: 14 March 2023), 2018. a
Amodei, M., Sanchez, I., and Stein, J.: Deterministic and fuzzy verification of the cloudiness of High Resolution operational models, Meteorol. Appl., 16, 191–203, https://doi.org/10.1002/met.101, 2009. a
Benamou, J.D. and Brenier, Y.: A computational fluid mechanics solution to the MongeKantorovich mass transfer problem, Numer. Math., 84, 375–393, https://doi.org/10.1007/s002110050002, 2000. a
Berchet, A., Sollum, E., Thompson, R. L., Pison, I., Thanwerdas, J., Broquet, G., Chevallier, F., Aalto, T., Berchet, A., Bergamaschi, P., Brunner, D., Engelen, R., FortemsCheiney, A., Gerbig, C., Groot Zwaaftink, C. D., Haussaire, J.M., Henne, S., Houweling, S., Karstens, U., Kutsch, W. L., Luijkx, I. T., Monteil, G., Palmer, P. I., van Peet, J. C. A., Peters, W., Peylin, P., Potier, E., Rödenbeck, C., Saunois, M., Scholze, M., Tsuruta, A., and Zhao, Y.: The Community Inversion Framework v1.0: a unified system for atmospheric inversion studies, Geosci. Model Dev., 14, 5331–5354, https://doi.org/10.5194/gmd1453312021, 2021. a
Bieser, J., Aulinger, A., Matthias, V., Quante, M., and Denier van der Gon, H.: Vertical emission profiles for Europe based on plume rise calculations, Environ. Pollut., 159, 2935–2946, https://doi.org/10.1016/j.envpol.2011.04.030, 2011. a
Bonneel, N., van de Panne, M., Paris, S., and Heidrich, W.: Displacement Interpolation Using Lagrangian Mass Transport, Association for Computing Machinery, New York, NY, USA, 30, 1–6, https://doi.org/10.1145/2070781.2024192, 2011. a
Broquet, G., Bréon, F.M., Renault, E., Buchwitz, M., Reuter, M., Bovensmann, H., Chevallier, F., Wu, L., and Ciais, P.: The potential of satellite spectroimagery for monitoring CO_{2} emissions from large cities, Atmos. Meas. Tech., 11, 681–708, https://doi.org/10.5194/amt116812018, 2018. a
Brunner, D., Kuhlmann, G., Marshall, J., Clément, V., Fuhrer, O., Broquet, G., Löscher, A., and Meijer, Y.: Accounting for the vertical distribution of emissions in atmospheric CO_{2} simulations, Atmos. Chem. Phys., 19, 4541–4559, https://doi.org/10.5194/acp1945412019, 2019. a
Cai, B., Cui, C., Zhang, D., Cao, L., Wu, P., Pang, L., Zhang, J., and Dai, C.: China citylevel greenhouse gas emissions inventory in 2015 and uncertainty analysis, Appl. Energ., 253, 113579, https://doi.org/10.1016/j.apenergy.2019.113579, 2019. a
Calvo Buendia, E., Tanabe, K., Kranjc, A., Baasansuren, J., Fukuda, M., Ngarize, S., Osako, A., Pyrozhenko, Y., Shermanau, P., and Frederici, S.: Quality Assurance/Quality Control and Verification, in: 2019 Refinement to the 2006 IPCC Guidelines for National Greenhouse Gas Inventories, vol. 1, IPCC, Switzerland, https://www.ipccnggip.iges.or.jp/public/2019rf/pdf/1_Volume1/19R_V1_Ch03_Uncertainties.pdf (last access: 14 March 2023), 2019a. a
Calvo Buendia, E., Tanabe, K., Kranjc, A., Baasansuren, J., Fukuda, M., Ngarize, S., Osako, A., Pyrozhenko, Y., Shermanau, P., and Frederici, S.: Uncertainties, in: 2019 Refinement to the 2006 IPCC Guidelines for National Greenhouse Gas Inventories, vol. 1, IPCC, Switzerland, https://www.ipccnggip.iges.or.jp/public/2019rf/pdf/1_Volume1/19R_V1_Ch06_QA_QC.pdf (last access: 14 March 2023), 2019b. a
Chen, Y., Georgiou, T. T., and Tannenbaum, A.: Optimal Transport for Gaussian Mixture Models, IEEE Access, 7, 6269–6278, https://doi.org/10.1109/ACCESS.2018.2889838, 2019. a
Chizat, L., Peyré, G., Schmitzer, B., and Vialard, F.X.: Scaling algorithms for unbalanced optimal transport problems, Math. Comput., 87, 2563–2609, https://doi.org/10.1090/mcom/3303, 2018. a, b
Crameri, F.: Scientific colour maps (7.0.1), Zenodo [code], https://doi.org/10.5281/zenodo.5501399, 2021. a, b
Davis, C. A., Brown, B. G., Bullock, R., and HalleyGotway, J.: The Method for ObjectBased Diagnostic Evaluation (MODE) Applied to Numerical Forecasts from the 2005 NSSL/SPC Spring Program, Weather Forecast., 24, 1252–1267, https://doi.org/10.1175/2009WAF2222241.1, 2009. a
Delon, J. and Desolneux, A.: A WassersteinType Distance in the Space of Gaussian Mixture Models, SIAM J. Imaging Sci., 13, 936–970, https://doi.org/10.1137/19M1301047, 2020. a
Denier van der Gon, H. A. C., Kuenen, J. J. P., JanssensMaenhout, G., Döring, U., Jonkers, S., and Visschedijk, A.: TNO_CAMS high resolution European emission inventory 2000–2014 for anthropogenic CO_{2} and future years following two different pathways, Earth Syst. Sci. Data Discuss. [preprint], https://doi.org/10.5194/essd2017124, in review, 2017. a
Dumont Le Brazidec, J., Bocquet, M., Saunier, O., and Roustan, Y.: Quantification of uncertainties in the assessment of an atmospheric release source applied to the autumn 2017 ^{106}Ru event, Atmos. Chem. Phys., 21, 13247–13267, https://doi.org/10.5194/acp21132472021, 2021. a
Ebert, E. E.: Fuzzy verification of highresolution gridded forecasts: a review and proposed framework, Meteorol. Appl., 15, 51–64, https://doi.org/10.1002/met.25, 2008. a
Ebert, E. E. and McBride, J. L.: Verification of precipitation in weather systems: determination of systematic errors, J. Hydrol., 239, 179–202, https://doi.org/10.1016/S00221694(00)003437, 2000. a
Farchi, A., Bocquet, M., Roustan, Y., Mathieu, A., and Quérel, A.: Using the Wasserstein distance to compare fields of pollutants: application to the radionuclide atmospheric dispersion of the FukushimaDaiichi accident, Tellus B, 68, 31682, https://doi.org/10.3402/tellusb.v68.31682, 2016. a, b, c
Feyeux, N., Vidard, A., and Nodet, M.: Optimal transport for variational data assimilation, Nonlin. Processes Geophys., 25, 55–66, https://doi.org/10.5194/npg25552018, 2018. a, b, c
Flamary, R., Courty, N., Gramfort, A., Alaya, M. Z., Boisbunon, A., Chambon, S., Chapel, L., Corenflos, A., Fatras, K., Fournier, N., Gautheron, L., Gayraud, N. T. H., Janati, H., Rakotomamonjy, A., Redko, I., Rolet, A., Schutz, A., Seguy, V., Sutherland, D. J., Tavenard, R., Tong, A., and Vayer, T.: POT: Python Optimal Transport, J. Mach. Learn. Res., 22, 1–8, http://jmlr.org/papers/v22/20451.html (last access: 14 March 2023), 2021. a
Gelbrich, M.: On a Formula for the L2 Wasserstein Metric between Measures on Euclidean and Hilbert Spaces, Math. Nachr., 147, 185–203, https://doi.org/10.1002/mana.19901470121, 1990. a
Gilleland, E.: Novel measures for summarizing highresolution forecast performance, Adv. Stat. Clim. Meteorol. Oceanogr., 7, 13–34, https://doi.org/10.5194/ascmo7132021, 2021. a
Gilleland, E., Ahijevych, D., Brown, B. G., Casati, B., and Ebert, E. E.: Intercomparison of Spatial Forecast Verification Methods, Weather Forecast., 24, 1416–1430, https://doi.org/10.1175/2009WAF2222269.1, 2009. a
Gilleland, E., Lindström, J., and Lindgren, F.: Analyzing the Image Warp Forecast Verification Method on Precipitation Fields from the ICP, Weather Forecast., 25, 1249–1262, https://doi.org/10.1175/2010WAF2222365.1, 2010. a
Hakkarainen, J., Szeląg, M. E., Ialongo, I., Retscher, C., Oda, T., and Crisp, D.: Analyzing nitrogen oxides to carbon dioxide emission ratios from space: A case study of Matimba Power Station in South Africa, Atmos. Environ. X, 10, 100110, https://doi.org/10.1016/j.aeaoa.2021.100110, 2021. a
Hergoualc'h, K., Mueller, N., Bernoux, M., Kasimir, A., van der Weerden, T. J., and Ogle, S. M.: Improved accuracy and reduced uncertainty in greenhouse gas inventories by refining the IPCC emission factor for direct N_{2}O emissions from nitrogen inputs to managed soils, Glob. Change Biol., 27, 6536–6550, https://doi.org/10.1111/gcb.15884, 2021. a
Hoffman, R. N. and Grassotti, C.: A Technique for Assimilating SSM/I Observations of Marine Atmospheric Storms: Tests with ECMWF Analyses, J. Appl. Meteorol. Clim., 35, 1177–1188, https://doi.org/10.1175/15200450(1996)035<1177:ATFASO>2.0.CO;2, 1996. a
Hoffman, R. N., Liu, Z., Louis, J.F., and Grassoti, C.: Distortion Representation of Forecast Errors, Mon. Weather Rev., 123, 2758–2770, https://doi.org/10.1175/15200493(1995)123<2758:DROFE>2.0.CO;2, 1995. a
Horowitz, C. A.: Paris Agreement, International Legal Materials, 55, 740–755, https://doi.org/10.1017/S0020782900004253, 2016. a
JanssensMaenhout, G., Crippa, M., Guizzardi, D., Muntean, M., Schaaf, E., Dentener, F., Bergamaschi, P., Pagliari, V., Olivier, J. G. J., Peters, J. A. H. W., van Aardenne, J. A., Monni, S., Doering, U., Petrescu, A. M. R., Solazzo, E., and Oreggioni, G. D.: EDGAR v4.3.2 Global Atlas of the three major greenhouse gas emissions for the period 1970–2012, Earth Syst. Sci. Data, 11, 959–1002, https://doi.org/10.5194/essd119592019, 2019. a
Kantorovich, L. V.: On mass transportation, C. R. (Doklady) Acad. Sci. URSS (N. S.), 37, 199–201, https://ci.nii.ac.jp/naid/10018386680/ (last access: 14 March 2023), 1942. a
Keil, C. and Craig, G. C.: A DisplacementBased Error Measure Applied in a Regional Ensemble Forecasting System, Mon. Weather Rev., 135, 3248–3259, https://doi.org/10.1175/MWR3457.1, 2007. a
Korsakissok, I. and Mallet, V.: Comparative Study of Gaussian Dispersion Formulas within the Polyphemus Platform: Evaluation with Prairie Grass and Kincaid Experiments, J. Appl. Meteorol. Clim., 48, 2459–2473, https://doi.org/10.1175/2009JAMC2160.1, 2009. a
Kuenen, J. J. P., Visschedijk, A. J. H., Jozwicka, M., and Denier van der Gon, H. A. C.: TNOMACC_II emission inventory; a multiyear (2003–2009) consistent highresolution European emission inventory for air quality modelling, Atmos. Chem. Phys., 14, 10963–10976, https://doi.org/10.5194/acp14109632014, 2014. a
Kuhlmann, G., Broquet, G., Marshall, J., Clément, V., Löscher, A., Meijer, Y., and Brunner, D.: Detectability of CO_{2} emission plumes of cities and power plants with the Copernicus Anthropogenic CO_{2} Monitoring (CO2M) mission, Atmos. Meas. Tech., 12, 6695–6719, https://doi.org/10.5194/amt1266952019, 2019. a
Kuhlmann, G., Brunner, D., Broquet, G., and Meijer, Y.: Quantifying CO_{2} emissions of a city with the Copernicus Anthropogenic CO_{2} Monitoring satellite mission, Atmos. Meas. Tech., 13, 6733–6754, https://doi.org/10.5194/amt1367332020, 2020. a
Lian, J., Wu, L., Bréon, F.M., Broquet, G., Vautard, R., Zaccheo, T. S., Dobler, J., and Ciais, P.: Evaluation of the WRFUCM mesoscale model and ECMWF global operational forecasts over the Paris region in the prospect of tracer atmospheric transport modeling, Elem. Sci. Anthr., 6, 64, https://doi.org/10.1525/elementa.319, 2018. a
Marzban, C. and Sandgathe, S.: Optical Flow for Verification, Weather Forecast., 25, 1479–1494, https://doi.org/10.1175/2010WAF2222351.1, 2010. a
Meinshausen, M., Meinshausen, N., Hare, W., Raper, S. C. B., Frieler, K., Knutti, R., Frame, D. J., and Allen, M. R.: Greenhousegas emission targets for limiting global warming to 2 ^{∘}C, Nature, 458, 1158–1162, https://doi.org/10.1038/nature08017, 2009. a
Menut, L., Bessagnet, B., Khvorostyanov, D., Beekmann, M., Blond, N., Colette, A., Coll, I., Curci, G., Foret, G., Hodzic, A., Mailler, S., Meleux, F., Monge, J.L., Pison, I., Siour, G., Turquety, S., Valari, M., Vautard, R., and Vivanco, M. G.: CHIMERE 2013: a model for regional atmospheric composition modelling, Geosci. Model Dev., 6, 981–1028, https://doi.org/10.5194/gmd69812013, 2013. a
Monge, G.: Mémoire sur la théorie des déblais et des remblais, Histoire de l’Académie royale des sciences avec les mémoires de mathématique et de physique tirés des registres de cette Académie, Imprimerie royale, 666–705, 1781. a
Nocedal, J. and Wright, S. J.: Largescale unconstrained optimization, Numerical Optimization, Springer, 164–192, ISBN 9780387303031, 2006. a
Peyré, G. and Cuturi, M.: Computational Optimal Transport: With Applications to Data Science, Foundations and Trends^{®} in Machine Learning, 11, 355–607, https://doi.org/10.1561/2200000073, 2019. a, b, c
Pison, I., Berchet, A., Saunois, M., Bousquet, P., Broquet, G., Conil, S., Delmotte, M., Ganesan, A., Laurent, O., Martin, D., O'Doherty, S., Ramonet, M., Spain, T. G., Vermeulen, A., and Yver Kwok, C.: How a European network may help with estimating methane emissions on the French national scale, Atmos. Chem. Phys., 18, 3779–3798, https://doi.org/10.5194/acp1837792018, 2018. a
Potier, E., Broquet, G., Wang, Y., Santaren, D., Berchet, A., Pison, I., Marshall, J., Ciais, P., Bréon, F.M., and Chevallier, F.: Complementing XCO_{2} imagery with groundbased CO_{2} and ^{14}CO_{2} measurements to monitor CO_{2} emissions from fossil fuels on a regional to local scale, Atmos. Meas. Tech., 15, 5261–5288, https://doi.org/10.5194/amt1552612022, 2022. a
Santaren, D., Broquet, G., Bréon, F.M., Chevallier, F., Siméoni, D., Zheng, B., and Ciais, P.: A local to nationalscale inverse modeling system to assess the potential of spaceborne CO_{2} measurements for the monitoring of anthropogenic emissions, Atmos. Meas. Tech., 14, 403–433, https://doi.org/10.5194/amt144032021, 2021. a, b
Seigneur, C.: Air Pollution: Concepts, Theory, and Applications, Cambridge University Press, ISBN 9781108481632, 2019. a
Solazzo, E., Crippa, M., Guizzardi, D., Muntean, M., Choulga, M., and JanssensMaenhout, G.: Uncertainties in the Emissions Database for Global Atmospheric Research (EDGAR) emission inventory of greenhouse gases, Atmos. Chem. Phys., 21, 5655–5683, https://doi.org/10.5194/acp2156552021, 2021. a
Super, I., Dellaert, S. N. C., Visschedijk, A. J. H., and Denier van der Gon, H. A. C.: Uncertainty analysis of a European highresolution emission inventory of CO_{2} and CO to support inverse modelling and network design, Atmos. Chem. Phys., 20, 1795–1816, https://doi.org/10.5194/acp2017952020, 2020. a
Tamang, S. K., Ebtehaj, A., van Leeuwen, P. J., Lerman, G., and FoufoulaGeorgiou, E.: Ensemble Riemannian data assimilation: towards largescale dynamical systems, Nonlin. Processes Geophys., 29, 77–92, https://doi.org/10.5194/npg29772022, 2022. a
Vanderbecken, P. J.: Passive gas plume database for metrics comparison (Version 0), Zenodo [data set], https://doi.org/10.5281/zenodo.6958047, 2022. a
Varon, D. J., Jacob, D. J., McKeever, J., Jervis, D., Durak, B. O. A., Xia, Y., and Huang, Y.: Quantifying methane point sources from finescale satellite observations of atmospheric methane plumes, Atmos. Meas. Tech., 11, 5673–5686, https://doi.org/10.5194/amt1156732018, 2018. a
Varon, D. J., Jacob, D. J., Jervis, D., and McKeever, J.: Quantifying TimeAveraged Methane Emissions from Individual Coal Mine Vents with GHGSatD Satellite Observations, Environ. Sci. Technol., 54, 10246–10253, https://doi.org/10.1021/acs.est.0c01213, 2020. a
Veefkind, J. P., Aben, I., McMullan, K., Förster, H., de Vries, J., Otter, G., Claas, J., Eskes, H. J., de Haan, J. F., Kleipool, Q., van Weele, M., Hasekamp, O., Hoogeveen, R., Landgraf, J., Snel, R., Tol, P., Ingmann, P., Voors, R., Kruizinga, B., Vink, R., Visser, H., and Levelt, P. F.: TROPOMI on the ESA Sentinel5 Precursor: A GMES mission for global observations of the atmospheric composition for climate, air quality and ozone layer applications, Remote Sens. Environ., 120, 70–83, https://doi.org/10.1016/j.rse.2011.09.027, 2012. a
Villani, C.: Optimal Transport, vol. 338 of Grundlehren der mathematischen Wissenschaften, Springer, Berlin, Heidelberg, https://doi.org/10.1007/9783540710509, 2009. a, b
For this specific value of ϵ, the d distance between 𝒰_{𝔼} and the first plume is similar to the d distance between the two plumes.
The convergence speed is measured here by the number of iterations.
By construction, X_{A} and X_{B} are normalised, in such a way that we do not need to renormalise them to be able to compute the Wasserstein distance.
If this is not the case, we just have to change θ_{A} to θ_{A}+π to swap σ_{1,A} and σ_{2,A}.
 Abstract
 Introduction
 Local metrics and illustration of double penalty issue using analytical plumes
 Metrics based on optimal transport theory
 Comparison of the metric on analytical test cases
 Comparison of the metric on realistic test cases
 Sensitivity to the meteorological conditions
 Conclusions
 Appendix A: LogSinkhorn algorithm
 Appendix B: Notations
 Appendix C: Gradient of the cost function for d_{F}
 Appendix D: From the Wasserstein distance w to the Hellinger distance w_{F}
 Code and data availability
 Author contributions
 Competing interests
 Disclaimer
 Acknowledgements
 Financial support
 Review statement
 References
 Abstract
 Introduction
 Local metrics and illustration of double penalty issue using analytical plumes
 Metrics based on optimal transport theory
 Comparison of the metric on analytical test cases
 Comparison of the metric on realistic test cases
 Sensitivity to the meteorological conditions
 Conclusions
 Appendix A: LogSinkhorn algorithm
 Appendix B: Notations
 Appendix C: Gradient of the cost function for d_{F}
 Appendix D: From the Wasserstein distance w to the Hellinger distance w_{F}
 Code and data availability
 Author contributions
 Competing interests
 Disclaimer
 Acknowledgements
 Financial support
 Review statement
 References