Mapping methane plumes at very high spatial resolution with the WorldView-3 satellite
- 1Research Institute of Water and Environmental Engineering (IIAMA), Universitat Politècnica de València, Valencia, Spain
- 2School of Engineering and Applied Sciences, Harvard University, Cambridge, MA, USA
- These authors contributed equally to this work.
Correspondence: Elena Sánchez-García (firstname.lastname@example.org)
The detection of methane emissions from industrial activities can help enable effective climate change mitigation strategies. These industrial emissions, such as from oil and gas (O&G) extraction and coal mining, typically occur as large plumes of highly concentrated gas. Different satellite missions have recently shown the potential to map such methane plumes from space. In this work, we report on the promising potential of the WorldView-3 (WV-3) satellite mission for methane mapping. This relies on its unique very high spatial resolution (up to 3.7 m) data in the shortwave infrared part of the spectrum, which is complemented by a good spectral sampling of the methane absorption feature at 2300 nm and a high signal to noise ratio. The proposed retrieval methodology is based on the calculation of methane concentration enhancements from pixel-wise estimates of methane transmittance at WV-3 SWIR band 7 (2235–2285 nm), which is positioned at a highly-sensitive methane absorption region. A sensitivity analysis based on end-to-end simulations has helped to understand retrieval errors and detection limits. The results have shown the good performance of WV-3 for methane mapping, especially over bright and homogeneous areas. The potential of WV-3 for methane mapping has been further tested with real data, which has led to the detection of 26 independent point emissions over different methane hotspot regions, such as O&G extraction fields in Algeria and Turkmenistan, and the Shanxi coal mining region in China. In particular, the detection of very small leaks (< 100 kg h−1) from oil pipelines in Turkmenistan shows the unique capability of WV-3 for mapping industrial methane emissions from space. The mission includes pointing capabilities that allow for a daily revisit over these oil pipelines or other critical infrastructure.
Widespread awareness of the accelerated increase of methane and other polluting gases in the atmosphere has heightened the need for new technologies to rapidly identify and control emission sources. During the last decades, increasing methane levels have been related to the rise of global warming risk. Reducing or stabilizing emissions would allow for a prompt decrease of atmospheric concentrations thanks to methane's relatively short lifetime of about 9 years (Saunois et al., 2020). Therefore, controlling the main contributors of methane emissions is seen as an effective option to mitigate climate change. Methane emissions from the fossil fuel industry represent a critical opportunity for mitigation, given the large number of uncontrolled emission point sources in oil and gas (O&G) and coal production areas worldwide (Jackson et al., 2020).
Substantial advances have been made in recent years towards the detection and quantification of methane point emissions from space (Jacob et al., 2016). The GHGSat satellite constellation was the first remote sensing system optimized for the monitoring of methane point emissions (Jervis et al., 2021) and is allowing the detection of a large number of anthropogenic methane emissions around the world, as shown in Varon et al. (2019, 2020). More recently, imaging spectrometers covering the entire 400–2500 nm region (known as hyperspectral land-surface imagers) have also shown their potential for mapping methane plumes from space such as the ZY1 AHSI, Gaofen-5 (GF5) AHSI, and PRISMA missions described by Irakulis-Loitxate et al. (2021, 2022) and Guanter et al. (2021). GHGSat and these hyperspectral missions share a relatively high sensitivity to methane concentration enhancements and a spatial sampling in the range of 25–50 m, but their acquisitions are sparse in time and space. The Sentinel-2 (S2) multispectral mission, also originally developed for land applications, can help to overcome this limitation with frequent and spatially continuous observations (Varon et al., 2021), albeit with a substantially lower sensitivity to methane. Landsat-7 and 8 missions, whose spectral channel configuration can provide a methane detection sensitivity comparable to S2 (see Fig. 1), offer the possibility of enlarging time series (Landsat-7 has operated since 2003). However, Landsat has a coarser spatial and temporal resolution (30 m vs. 20 m, and 15 d vs. 5 d) compared to S2. Methane mapping efforts with all those missions greatly benefit from the synergistic use of the TROPOspheric Monitoring Instrument (TROPOMI) onboard the Sentinel-5 Precursor satellite (Hu et al., 2018; De Gouw et al., 2020; Lauvaux et al., 2022). TROPOMI data allow identifying regions with strong methane concentration enhancements (Sadavarte et al., 2021), where the aforementioned missions can focus on the detection of single emitters.
The present work describes a new breakthrough in this quickly developing field towards the global mapping of methane point emissions. Using very high-resolution shortwave infrared (SWIR) measurements from the WorldView-3 (WV-3) satellite, we have mapped methane plumes from different locations around the Earth at a spatial resolution of 3.7 m (European Space Imaging, 2020). Positive plume detections have been obtained from O&G extraction fields in Algeria and Turkmenistan, and the Shanxi coal mining region in China. Until now, methane retrievals at such high-resolution were only possible for airborne instruments, like the AVIRIS and AVIRIS-NG spectrometers operated by NASA JPL (Frankenberg et al., 2016; Jongaramrungruang et al., 2019; Cusworth et al., 2019; Duren et al., 2019). The WV-3 instrument combines a high spatial resolution with a high signal-to-noise ratio (SNR) and rich spectral coverage of the strong methane absorption feature around 2300 nm (see Fig. 1). Furthermore, the onboard system includes pointing capabilities that are able to deliver a daily revisit or better over critical infrastructure. These unique features allow WV-3 to fill an important observational gap in international satellite methane monitoring capabilities.
Mapping methane emissions at this very high spatial resolution enables a substantial improvement of emission detection thresholds. Accurate identification of the particular infrastructure elements responsible for the emissions and more precise quantification of emission rates is also made possible by the unprecedented spatial resolution of WV-3.
2.1 Methane retrieval
Methane retrieval algorithms for hyperspectral instruments typically estimate methane concentration enhancement by fitting highly resolved observations in the SWIR spectral region to a modeled radiance spectrum (Thorpe et al., 2014; Jacob et al., 2016). In a single overpass, hyperspectral instruments onboard satellites or aircraft can resolve the SWIR spectral region with a typical spectral resolution ranging from 0.1 to 15 nm.
For multispectral instruments like S2, Landsat, and WV-3, the entire SWIR spectral region cannot be resolved. Nonetheless, it is possible to retrieve methane concentration enhancements within an image from differences in methane transmittance between spectral bands. To calculate methane transmittance, we normalize the radiance at a spectral channel affected by methane absorption by a “methane-free” reference band, i.e., with no excess methane. In the absence of multitemporal data, this reference can be built from one or several neighboring channels that are mostly insensitive to excess methane. WV-3 contains a richer spectral design with 8 SWIR bands at 3.7 m spatial resolution (see Fig. 1) and narrower bandwidth as compared to the S2 and Landsat missions. Specifically, it contains two bands (B7 and B8) in regions of strong methane absorption and spectrally close bands (B5 and B6) at less than 100 nm separation (as opposed to the 600 nm spectral distance between S2 B11 and B12 bands). WV-3 images in the SWIR are processed with a time-delayed-integration (TDI) of 16 lines. TDI refers to the exposure of the same area multiple times by different pixels in the detector as the satellite is moving along the orbit. These measurements can be added and consequently improve the noise of the image. This contributes to a superior SNR as compared to other multispectral missions such as S2 (the latter includes TDI of 2 lines in the SWIR bands).
Thus, the proposed rationale to detect methane plumes is based on an estimation of the plume transmittance defined by the ratio of a methane-sensitive band such as WV-3 B7 or B8 with excess methane present, and the corresponding “methane-free” reference band. Mathematically, the plume transmittance Tplume can be described as
where L and Lref represent the radiance of the methane-sensitive band and the “methane-free” reference band respectively. AMF refers to the geometric air mass factor, (ppm−1) refers to the methane absorption cross section, and ΔXCH4 (ppm) refers to the methane column concentration enhancement. The latter expresses the increment produced by the plume from the background methane present in the atmospheric column.
We have tested that both the spectral response function (SRF) knowledge and water vapor absorption constitute minor sources of uncertainty in the estimation of Tplume. The sensitivity study setup a reference scene with a simulated methane plume (Q = 1000 kg h−1). In order to test the impact of the SRF knowledge on the methane retrieval, the SRF central wavelength has been shifted for the convolution of the methane transmission. A shift of ±5 nm has been selected as a “typical” tolerance of a multispectral mission design. The results show that the impact of spectral shifts on B8 is lower than 1 % and larger errors were observed in B7 (up to 8 %) due to the larger changes in methane absorption within this band. The water vapor column has been modified in a range from 0 to 40 mm representative of extreme values in the atmosphere. The results for water vapor errors can reach up to 5 % for B8 and just 1 % for B7.
The approach to obtain the Lref “methane-free” reference band (L in the absence of excess methane) is based on the idea that this could be approximated using other spectral channels that are mostly insensitive to excess methane. The simplest form of this model would be the ratio between B7 and B5, which are spectrally close and correlated (see Fig. 1).
From the several options that have been considered (see Fig. 6), the selected method for the estimation of this “methane-free” band is based on a multiple linear regression (MLR) of B1–B6 with B7 as the target band (B7 B7MLR method). Despite B8 being more sensitive to methane absorption, this band has shown lower spectral correlation with B1–B6 bands as compared to B7 (see results in Sect. 3.1). Out of the six bands considered for the regression, three of them (B3, B5, and B6) are marginally sensitive to methane. In the case of B3, its weight on the regression is small and has negligible impact, and thus we do not include this band. However, in the case of B5 and B6, their spectral closeness to B7 improves the regression and outweighs the impact that the residual methane sensitivity of these bands produces on the retrieval. The effect of B5 and B6 on the retrieval performance was tested by producing a set of simulations that do not incorporate the methane plume transmittance on these two bands. The performance of these fit-for-purpose products was compared to the full end-to-end simulated products. We find that including these spectral bands with partial methane sensitivity in the MLR reduces the integrated methane enhancement (IME; total excess methane mass; Frankenberg et al., 2016) of retrieved plumes by roughly 7 %.
The methane plume quantification with WV-3 is obtained by isolating the methane column enhancement in Eq. (1). Then, ΔXCH4 becomes a function of the AMF and the radiance ratio of SWIR B7 (2235–2285 nm). A look-up table (LUT) can be generated so that the relationship between these two quantities and the methane enhancement is established and expressed as follows:
Figure 2 shows the LUT relationship between the methane plume transmittance and the methane column enhancement (ΔXCH4) for different values of AMF. The figure also highlights the optimized spectral design of WV-3 with respect to other multispectral missions, such as S2. It illustrates how both WV-3 B7 and B8 cover a wider range of plume transmittance values as compared to S2 band 12. Furthermore, it shows how the sensitivity increases with the AMF values, although this is at the expense of potential shadowing and surface directional effects (Guanter et al., 2021).
2.2 Detection of methane plumes
The detection of methane plumes begins with the visual inspection of the retrieved ΔXCH4 maps. It is generally easy to distinguish the plumes from the background in the retrieved maps due to the low random noise and the characteristic shape of the plumes. This noise is generated by the inherent instrument noise, misregistration between the bands, and several surface features that complicate the retrieval by having a similar spectral signature to methane. Once the plumes have been initially identified, it is checked that their shape is consistent with the Goddard Earth Observing System-Fast Processing (GEOS-FP) 10 m wind direction data. That is, the shape of a gas plume is expected to originate at high ΔXCH4 values and decrease progressively downwind. Once the plumes have been verified, they are collocated with high spatial resolution true color images of the area in order to identify the underlying infrastructure responsible for this emission. For this process, we use Google Earth images and the first SWIR band (B1 ∼ 1200 nm) of the WV-3 images.
The next step of the detection processing zooms in on each real plume to isolate it from the background in order to compute the total area covered by the emission. The methodology proposed in Thompson et al. (2016) is based on a statistical significance of a rectangular region of 500 samples directly upwind of the plume, while Varon et al. (2018) use the statistical significance (p≤0.05) associated with a 5 × 5 window Student's t-test. In both cases, a median filter is set to smooth the plume mask and remove outliers.
Here, a semi-automatic process has been implemented, where the plume is isolated by applying a mask at the 95 % confidence level and a square dilation mask of several pixels a posteriori. Similarly to the median filter, a mask dilation ensures that plume tails are included in the detected area. Moreover, it guarantees a plume selection with a reduced number of discontinuities as expected from the spatial distribution of a gas plume. Finally, the detected outliers in the vicinity of the plumes are removed through feature selection techniques. These, such as clustering properties and blob detection measures, automatically identify the features in the image, which are further filtered out based on their properties, such as number of pixels or eccentricity. Techniques that allow us to get a kind of image classification to detect the plume shape and remove those features that, despite its high ΔXCH4 values, are not part of the emission. Sometimes, the radiance of the satellite bands is also used in this discrimination process.
2.3 Estimating emission flux rates
Once the plumes have been identified, the associated flux rate Q is obtained by applying an IME method (Frankenberg et al., 2016; Varon et al., 2018). The ΔXCH4 values are converted from ppm to ppm m units and to kg (Thompson et al., 2016; Duren et al., 2019) by considering the 3.7 m of WV-3 pixel spatial resolution, Avogadro's law where 1 mole of gas occupies 22.4 L, the estimation of 0.01604 kg per mole of methane, and a factor of 8000 that accounts for the column height assuming an atmosphere of 8 km. Then, we compute IME in kg for each plume as the total sum of the ΔXCH4 pixels enclosed by the plume mask. The last step relates the emission flux rate with the calculated IME as
where L is a plume length scale in m (square root of the entire area covered by the plume pixels), and Ueff the effective wind speed derived from Weather and Research Forecasting Model large-eddy simulation (WRF-LES) according to Varon et al. (2018) methodology.
For this study, the WRF-LES simulations were tuned at the spatial resolution and measurement uncertainty of WV-3 (∼ 4 m resolution and 1σ white noise varying from 120 to 370 ppb depending on the site; see Fig. 8). Then, six IME calibrations were performed for each of these three 1σ noise levels and considering two different emission ranges: kg h−1 and kg h−1. Figure 3 shows the fits obtained for the extreme cases out of the six IME calibrations, which correspond, respectively, to σ=120 ppb and kg h−1 (the highest signal case), and to σ=370 ppb and kg h−1 (the lowest signal case).
The similarity achieved between the six individual fits leads to the adoption of the following formula that considers the middle values of the coefficients obtained from the calibrations:
In this proxy, the measurable 1 h average 10 m wind speed (U10) derives from the two north–south and east–west wind components of GEOS-FP dataset (https://portal.nccs.nasa.gov/datashare/gmao/geos-fp/das/, last access: 15 March 2022) at the satellite acquisition time and for the location of each plume. Consider that GEOS-FP is a meteorological reanalysis product with a resolution of 0.25∘ × 0.3125∘ (Molod et al., 2012).
Consider that the definition of L affects the shape of the Ueff=f(U10) relationship, so the reason we need such low Ueff values here (much lower than U10) is because the area of plume mask is very low for thin, high-resolution plumes. In addition, this calibration has been set for small plumes because the LES model domain is only ∼ 200 m across. Then, this would be expected not to be accurate for larger plumes causing underestimates of Q because these plumes, even sampled at 4 m resolution, are transported over a much larger part of the boundary layer than the small ones. Therefore, the Ueff calibration set for PRISMA in Guanter et al. (2021) is used for those plumes over 200 m in length.
For each Q value, we have estimated an associated uncertainty similarly to the method used in Cusworth et al. (2020), Guanter et al. (2021), and Irakulis-Loitxate et al. (2021, 2022). The uncertainty formalism is based on a Monte Carlo propagation (JCGM, 2008) of the uncertainties in IME, U10, and the coefficients of Eq. (4) through Eqs. (3)–(4). Here, the uncertainty of the input U10 is set to a conservative 50 % uncertainty k=11 estimate in GEOS-FP U10 data consistent with the ∼ 1.5 m s−1 error standard deviation in wind speed given by Varon et al. (2020). The uncertainty in the IME is calculated based on the uncertainty combination of different pixels with an associated “retrieval noise”. This is the consequence of instrument noise, misregistration, and surface heterogeneity. Finally, an uncertainty k=1 of 0.01 for both the slope and intercept of Eq. (4) is included in the Monte Carlo propagation. This is a proxy of the regression sensitivity to different scenarios such as different flux rate ranges or noise levels previously discussed.
The different error samples in the Monte Carlo propagation have been treated as uncorrelated. This can be justified because there is no expected relationship between the errors in IME, U10, and the intercept/slope in Eq. (4), as they are largely obtained from independent processes. A weak correlation of ∼ 0.28 between the slope and intercept errors in Eq. (4) has been empirically determined but considered to be of negligible impact on the overall budget. The result of the Monte Carlo propagation is an error distribution associated with the calculated Q value. The standard deviation of this error distribution is considered the uncertainty k=1 for the Q of each plume under the assumption of a normal distribution. Both the accuracy of the IME model and its relationship with the length scale L of the plume are considered to be out of the scope of this work.
2.4 Sensitivity analysis based on end-to-end simulations
The potential of WV-3 for methane mapping has been assessed through a sensitivity analysis based on end-to-end simulations. The simulations are generated by convolving WV-3 TOA radiance scenes with synthetic methane plumes generated with the WRF-LES.
The WRF-LES simulations are set at 30 m × 30 m spatial resolution, 100 W m−2 sensible heat flux and a mean wind speed of 3.5 m s−1 as in Cusworth et al. (2019). These original plumes are upsampled to 3.7 m in order to match the spatial resolution of WV-3. The plumes are further scaled from an initial source rate Q of 100 kg h−1 to the desired flux. The upsampling and scaling of the reference plume has no effect on the sensitivity analysis but a small interpolation effect that generates a second-order error. An example of the resulting methane plume is shown in Fig. 4 with a Q of 1000 kg h−1.
Similarly to Cusworth et al. (2019), the spectral optical depth of the methane plume τ(λ) is calculated as the sum of 72 layers of the atmosphere. At each layer, we multiply the HITRAN absorption cross sections (σH; Kochanov et al., 2016), the vertical column density of dry air (VCD), and the methane volume mixing ratio enhancement (ΔVMR). The optical depth is weighted by the AMF that considers the slant optical path due to both the illumination and viewing angular conditions. We obtain a methane plume transmittance map at a fine spectral resolution by applying Beer's law. Finally, this fine spectral resolution map is convolved with the WV-3 SRF, and the result is a methane plume transmittance map for each one of the WV-3 spectral bands.
The calculated plume transmittance for each band is multiplied by the observed radiance at each one of the respective bands. This results in simulated methane plume products that incorporate a real scene from WV-3 with realistic surface, instrument noise, or viewing effects among others. The a posteriori convolution of the band radiance with the plume transmittance produces a small bias that is partially compensated.
The end-to-end simulations have been generated for three different sites in Algeria, Turkmenistan, and China whose spectral response behave differently regarding their surface conditions (see Fig. 5). The WV-3 images used for the simulations were acquired on 29 December 2020 in Algeria, 27 April 2021 in China, and 29 March 2021 in Turkmenistan. Figure 5 displays in the top row an RGB snapshot of the three sites. The area defined by the red square on the RGB snapshots shows the WV-3 SWIR B7 subsets displayed at the bottom row of the figure, which are the ones used for the end-to-end simulations.
Among the chosen sites, the one in Turkmenistan shows the lowest spatial variations in the SWIR B7, whereas the one in China is expected to be the most challenging site for methane plume detection due to its higher spectral and spatial heterogeneity. The Algeria site covers a largely homogeneous area similar to Turkmenistan, although it contains some cirrus/cloud shadows at the right half of the selected subset that alter the radiance in SWIR B7.
Finally, it is important to remark that the sites selected for the simulations are realistic insofar as they are well-known areas of O&G and coal production facilities with known methane emissions (Irakulis-Loitxate et al., 2021, 2022; Varon et al., 2021; Cusworth et al., 2021).
3.1 Retrieval performance with simulated plumes
The end-to-end WV-3 simulations defined in Sect. 2.4 have been used here to test the performance of different methane retrievals. Figure 6 presents the ΔXCH4 maps at two sites that result from the application of different approaches to calculate a “methane-free” reference band. The retrieval using a radiance ratio of B8 against the MLR of B1–B6 with B8 as the target band shows the largest sensitivity as compared to the other two retrievals using B7. However, the result also exhibits a pronounced impact of outliers (e.g., the dunes in Turkmenistan or the roads in Algeria) due to the larger spectral distance from B8 and B1–B6. The results using a radiance ratio of B7 against the MLR of B1–B6 and that of a single ratio of B7 against B5 present similar results. Nonetheless, the former results in a clear shape of the plume and a slight decrease of outliers. Thus, the calculation of the plume transmittance as a radiance ratio of B7 against the MLR of B1-B6, described in Sect. 2.1, is selected as the best compromise between detection sensitivity and low outlier generation.
The methodology selected has been performed with the end-to-end simulations at various sites and for different Q levels. The method takes the radiance ratio B7 B7MLR, which defines a proxy of the methane plume transmittance that can be associated with a methane enhancement value according to Beer's law. Different flux rates have been simulated leading to a set of ΔXCH4 maps that have been further processed in order to isolate the plume from the background, as explained in Sect. 2.2.
Figure 7 displays the retrieved ΔXCH4 maps for an input flux rate of 500 and 2000 kg h−1 at the three sites of study. A simple glance at the enhancement maps suggests that the best results are obtained in the Turkmenistan and Algeria sites. The Algeria maps show a discontinuity on the right-hand side of the image. This effect could be caused during the WV-3 product processing due to focal plane discontinuities. Different collection scenarios are considered in the VW-3 mission, which include the generation of an image with different overpasses each with a swath of 13.1 km. Based on the results presented here, this effect must be considered a minor one largely due to the spectral correlation nature of the error. Nonetheless, this effect is compensated in the results presented in Sect. 3.2. Finally, the enhancement maps of China present many features that alter the retrieval and require higher methane plume signals in order to positively detect them.
The performance of the retrieval is easier to understand if we attend to the background noise of the ΔXCH4 maps. Figure 8 shows the distribution of the retrieved ΔXCH4 maps for the three sites presented in Sect. 2.4. The data represents a subset of 600 × 600 pixels of the original images. The histograms indicate the variation of the noise levels across the different sites from a low level of 120 ppb in Algeria up to 370 ppb in China (1σ retrieval errors used to set Eq. 4). These values, as expected, are sensibly larger than other missions with a lower spatial resolution due to the increased surface variability. For example, the retrieval noise reported by Guanter et al. (2021) using PRISMA data is almost half of the values shown here for similar sites. Another observed difference is the non-normal nature of the retrieval noise in WV-3 (the same plots for the retrieval noise in PRISMA show an almost perfect Gaussian fit). Further investigation has concluded that this non-normal behavior is not produced by any step in the retrieval itself but is present in the radiance ratio . Different ratios were investigated, all producing a non-normal distribution, and it remains even after applying a spatial binning to, e.g., 30 m. Thus, it is likely that this non-normal behavior is the consequence of a noise pattern between B7 and the rest of the bands (e.g., due to the large number of TDI stages which might enhance the prevalence of non-normal effects). However, it requires a better understanding of the calibration and instrument specifications that are not currently available.
The methane plumes presented in Fig. 7 have been isolated from the background considering the noise levels in Fig. 8, and the procedure explained in Sect. 2.2. Figure 9 displays the relationship between the retrieved IME values and the known reference input for the simulations at the three sites. The IME is calculated from a reference mask at each flux rate level. This typically results in smaller plumes, with lower IME than the reference, since we attempt to reconstruct that mask in the presence of noise. The simulations in China, Turkmenistan, and Algeria were performed at a Q step size of 100 kg h−1. The results highlight a general underestimation of the retrieved IME values, i.e., smaller plumes with lower IME than the reference. For example, considering an input flux rate of 1000 kg h−1, the results show an IME underestimation of 22 % for Algeria, rising up to 61 % for the case of China. The missing fractions of the total IME are larger at all input levels for the China case, and the lowest fraction is associated with the Algeria simulations. This is a similar result to other studies, such as Guanter et al. (2021), and comes to reinforce the importance of surface heterogeneity on the performance retrieval. It is important to remark that the IME loss scales, in absolute values, with the value of simulated Q. However, in relative terms, this loss tends to become smaller.
3.2 Real case studies of methane detection
Different ΔXCH4 maps are presented here derived from real WV-3 images. We work with a total of seven SWIR WV-3 images covering four different areas in Algeria, Turkmenistan North and Turkmenistan South (both methane hotspot regions located near the shores of the Caspian Sea, in western Turkmenistan), and China. In the case of Algeria, two images of 25 km2 area each belonging to the Hassi Messaoud oil field have been processed; the eastern one was acquired on 29 December 2020, and the western one was acquired on 17 January 2021. The image in Turkmenistan North corresponds to the Goturdepe O&G extraction field, where two images of 50 km2 each were acquired on 10 April 2021 (Eastern area) and 29 March 2021 (Western area). The Turkmenistan South site (near the mud volcanoes area) contains the Korpezhe O&G field, where two more images of 50 km2 each were acquired on 29 March 2021 for both eastern and western areas. Finally, we present an image of the Shanxi coal mines in China (west of the Zhangze reservoir) that covers an area of 25 km2 and was tasked for acquisition on 27 April 2021.
All of these areas correspond to known regional methane hotspots where TROPOMI commonly detects substantial methane concentration enhancements (Lauvaux et al., 2022) but without succeeding in detecting the sources due to their moderate resolution.
∗ The flux rate Q on these two methane plumes is computed considering half IME and half of the number of pixels due to the particular dual-plume structure caused by the angular configuration for that day (see Fig. 11).
Our results with WV-3 reveal the precise locations of 26 different point source emissions (listed in Table 1) over the total area of 275 km2 analyzed. Accurate coordinates of each point source are provided thanks to the high spatial resolution of WV-3 SWIR images and, in combination with the Google Earth imagery (< 2.5 m per pixel), that provides enough information to determine the underlying infrastructure responsible for the emission. From the calculation of the IME, we derived the Q values estimated for all plumes as presented in Sect. 2.3. The plumes presented here range from the 30 kg h−1 emission flux rate and 50 m length plume detected in Turkmenistan North (western image) to the massive emission flux rate of 35000 kg h−1 extending up 2 km in Turkmenistan North (eastern image).
Each flux rate Q in Table 1 incorporates an attached uncertainty k=1, which is the result of the Monte Carlo propagation formalism described in Sect. 2.3. These uncertainties cover a range of 15 % to 45 %, which is a substantially lower figure compared to other missions such as PRISMA (Guanter et al., 2021). The main factor of disagreement resides in the different slope values of the U10–Ueff relationship applied to plumes with L lower than 200 m. The slope associated to PRISMA is 0.34, whereas the simulations for WV-3 result in a slope of just 0.12 (see Eq. 4). The uncertainty of U10 is, at the moment, the dominant uncertainty source and, thus, the lower slope coefficient for WV-3 contributes to the lower Q uncertainty.
The fact that Ueff (or U10) represents the dominant source of uncertainty is studied in Fig. 10. It shows the sorted Q values in ascending order at the bottom panel with the associated relative uncertainty for each plume at the top panel. The figure captures an uncertainty trend associated to the Q level with a small correlation of 0.45. The same ordering methodology has been replicated for the IME and Ueff values. The results showed a weak correlation of the Q uncertainty with the IME value (∼ 0.15) and a high correlation (∼ 0.85) of the Q uncertainty with the Ueff.
Figures 11–15 showcase the methane plumes listed in Table 1 as part of the retrieved methane enhancement maps of the studied areas. In some cases, the methane plumes have been cropped, and the WV-3 SWIR B1 band has been integrated as a background scene for visual identification of the underlying infrastructure. Figure 11 displays the ΔXCH4 map from Turkmenistan South on 29 March 2021 at the left panel. This map includes two plumes that are zoomed in and displayed with the WV-3 SWIR B1 background. These two methane plumes present a particular shape as a consequence of the orthogonal alignment of the sun-to-satellite plane with respect to the wind direction (Fig. 11 includes a schema of the angular configuration). This particular angular configuration enhances the parallax effect introduced by the plume at a certain height and is translated into two different plume projections (sun and surface reflected paths) that are clearly visible in Fig. 11b. This example is similar to the dual-plume structure described in Borchardt et al. (2021) for AVIRIS-NG and comes to reinforce the importance of geometric considerations for high-spatial methane quantification. Furthermore, the particular angle configuration in Fig. 11 also enhances the effect of soil morphology visible throughout the entire ΔXCH4 map as a NW-SE streak noise pattern. Despite the geometric and soil morphology effects, both emission sources are easily distinguished by the high ΔXCH4 values and the unmistakable diffuse shape of the tail downwind. These two emitter points have already been registered by Irakulis-Loitxate et al. (2022). The massive southern plume extends up to 3 km as shown in the enhancement map of Fig. 11, in particular, inside the white box called “(b)” at the left panel. However, the retrieved mask used to calculate the IME and associated flux rate Q only takes the most integral part of the plume, as the zoomed map in Fig. 11b shows. Moreover, because of the parallax effect, only half of each plume mask would be considered for flux rate Q estimates. This plume emerges from a gas pipeline near the compressor station already reported by Varon et al. (2019, 2021) and Irakulis-Loitxate et al. (2022). Despite the first announcement in Varon et al. (2019) and subsequent shutdown of the leak, it is here shown that this emitter source is once again spreading methane to the atmosphere. On the North area of the left panel in Fig. 11, another plume with a flux rate four times smaller is also detected. Both points are classified as O&G ground flare emitters that are often used in the burning of gaseous waste and whose installation is distinguishable on the images.
The area with the largest number of emitters in this study corresponds to the Goturdepe O&G field and is located in the north of Turkmenistan. A total of 16 different plumes have been detected throughout this basin, one of the oldest oil piping systems in Turkmenistan. The top panel in Fig. 12 shows the methane enhancement map for the Eastern image on 10 April 2021. Two elongated plumes (consequence of strong wind; see Table 1) are highlighted in the image inside a white rectangular box. The plumes originate from two-point sources – registered also in Irakulis-Loitxate et al. (2022) – where the dark color of the soil in the 2021 Google Earth RGBs images indicate that oil burning works are taking place in the area. The biggest plume (Fig. 12a) emerges from a thin pipeline coming out of the adjoining oil power plant. The origin of the other plume (Fig. 12b) is not so obvious but is likely caused by leakage from the piping system affecting the area.
The image covering the latter area of the North of Turkmenistan on 29 March 2021 is perhaps the most interesting one because of the number of small methane leakages that WV-3 has been able to reveal (see Fig. 13b). Looking at first glance at the ΔXCH4 map, an apparent single plume at the well-known point northwest of the image (Irakulis-Loitxate et al., 2022) can be glimpsed, as well as another plume towards the center of the image. However, by zooming in closer and considering the wind direction on that day, it has been possible to disentangle each of the underlying and independent emitting points for each case and even unfolding those principal sources. For example, observing this apparent first northwest plume near coordinates 39.498∘ N, 53.636∘ E, just a few meters away, there is found a second emitter point at the northern end of the same pipeline where a ground flare is perceived. WV-3 data makes it possible to clearly attribute these two emitting points to separate pieces of infrastructure, even if their tails intertwine later downwind. The same occurs with the plume seen towards the image center near coordinates 39.485∘ N, 53.663∘ E. This plume is, in fact, subdivided into four sources from different leakage points along an oil pipeline, shown zoomed-in in Fig. 14. Following its route to the southeast, we come across other methane plumes and quite a few smaller ones among the pipeline crossings to the south up to 50 m in length and a flux rate Q of about 30 kg h−1.
Some of the small leaks illustrated in Fig. 13b would go unnoticed by most satellites with lower spatial resolution and worse specifications for methane detection. Particularly those small plumes registered in the gray box area of roughly one square kilometer at the bottom right of the image.
Figure 14 exemplifies this fact by upsampling the real image from 3.7 to 30 m per pixel and showing how the different point leakages would not be identified at coarser resolution and would subsequently be registered as a single plume instead of four independent sources. The ability to precisely locate and identify these emitting points could help steer the decision-making process for repairing such pipeline leaks, delivering strong environmental and socioeconomic impacts.
Regarding the image in Algeria on the 29 December 2020, despite optimal surface conditions, the results show a radiance jump around the middle of the image, as was already discussed in Sect. 3.1. This typically occurs when the WV-3 mission acquires the product with overlapping scans, each with small differences (e.g., viewing geometry). Despite its relatively narrow swath of 13.1 km, it incorporates an agile pointing system capable of collecting stacked stripes at different scans over the same area. In order to overcome this issue, the methane retrieval was processed separately for each part of the image. Figure 15 shows the resulting methane enhancement map where the visual results have clearly improved and just a residual effect at the fringes of the transition area. On this day three elongated plumes emerging from different pipelines are almost perfectly aligned with wind direction, and with emission concentration values steadily decreasing due to the relatively high wind speed (6.14 m s−1). This high wind speed produces a fast dispersion of the plume at about 500 m travel, blurring until the plume tail disappears. On the contrary, on days with low wind speeds (2.37 m s−1), as on 17 January 2021 (see the example in Fig. 13a), the high concentrations of the gas remain concentrated near the emitting point defining a shorter plume.
To further demonstrate the value of methane plume detection at 3.7 m pixel resolution, Fig. 15 shows the ΔXCH4 map obtained from the Algeria image on 29 December 2020 (see the isolated plumes in Fig. 13a) and compares it with this same result but upsampled to 30 m resolution, similarly to Fig. 14. With this coarser resolution, apart from blurring the emitter point, the plumes become more difficult to define, especially the smaller one, which is easily confused amid the background noise.
Moreover, the high spatial resolution of WV-3 has not only been helpful to identify small sources of methane emissions but also to detect outliers. Based on the idea that a methane plume in the atmosphere is characterized by soft edges, whereas the presence of other features such as buildings and roads typically result in sharp edges, it has been possible to apply feature detection techniques as described in Sect. 2.2.
This study reveals the previously undocumented capability of WV-3 for mapping methane point source emissions at very high spatial resolution. The retrieval methodology is based on the MLR of 6 SWIR bands with low sensitivity to methane absorption against B7 (2235–2285 nm), which is positioned at a highly-sensitive methane absorption region. The ratio between the original B7 band and the band obtained through the regression results in an estimated methane plume transmittance that links to the column-averaged mixing ratio (ΔXCH4). The study found a weak sensitivity of the methane retrieval to the SRF of B7 and a negligible effect to the atmospheric water vapor column. Although WV-3 B8 (2295–2365 nm) is at a stronger methane absorption position than the rest of the bands, our methodology proved to retrieve better results using B7 as a reference due to its higher spectral correlation with the rest of the SWIR bands.
The unprecedented spatial resolution of WV-3 combined with its high-quality spectral configuration and relatively low noise enables the detection of even smaller plumes than detected by hyperspectral missions (∼ 30 m pixel resolution) and other multispectral missions such as S2 (20 m pixels). Furthermore, this mission includes unique pointing capabilities that can optimize acquisition over O&G fields by tracking directly over suspected areas of point emitters with a daily revisit or better (European Space Imaging, 2020).
The resulting ΔXCH4 maps obtained with our methane retrieval from WV-3 SWIR images have identified different uncontrolled gas leaks in two different O&G extraction regions in Turkmenistan and Algeria, which in some cases come directly from the production facilities and in others are due to ruptures of the natural gas pipelines, and some emissions in the Shanxi coal mining region in China. The precise detection and identification of these emitters enables direct action to mitigate them. Our results show how we can pinpoint small emissions along oil pipelines (< 100 kg h−1) as shown in Fig. 13 and Fig. 14 for a 10 m wind speed of 1.84 m s−1, illustrating the unique capability of WV-3 for methane mapping from space. WV-3 has a superior detection limit to other multispectral satellite missions, comparable in some cases to airborne spectrometers.
The end-to-end sensitivity analysis of the methane retrieval with WV-3 and for a mean wind speed of 3.5 m s−1, has shown excellent results over homogeneous surfaces. The IME loss for methane sources over an O&G extraction region in Algeria was as low as ∼ 20 kg (22 % loss for a flux rate of 1000 kg h−1). For highly heterogeneous areas such as the scene in Shanxi, China, larger fractions of the IME can be lost (up to 61 %, or ∼ 54 kg for a flux rate of 1000 kg h−1). In terms of detection thresholds, these results for a 3.5 m s−1 wind speed indicate that a flux rate of 200–300 kg h−1 can be detected over sites such as Algeria and Turkmenistan, and rising to ∼ 600 kg h−1 for the site in China.
Despite the promising results shown in this first assessment of WV-3 for monitoring and quantifying methane plumes, further work is needed to diminish the impact of the surface background and the plume parallax effects on the derived methane concentration enhancement maps. The former issue is shared with other missions, but in the case of WV-3 it becomes critical due to the higher variability of the surface at 3.7 m sampling and its orbit pointing capabilities that can result in large viewing zenith angles. The latter issue is enhanced at angular configurations such as the one presented in the example of the Korpezhe O&G field in Fig. 11. In the case of the plume parallax effect, 3-D information about the plume structure is needed to estimate a path at a pixel-level that supports a more accurate quantification. The surface variability could be mitigated if further development of the retrieval includes knowledge of the surface local angle information (e.g., through a high spatial resolution digital elevation model). In addition to the SWIR bands, the WV-3 mission also images the VNIR TOA radiance with 1.24 m spatial resolution at nadir. A combination of the SWIR images with this VNIR data could improve both the regression and the identification of emission infrastructure. Moreover, both the simulations and real cases investigated here are for an acquisition period between October 2020 and April 2021 characterized by a lower SZA around the winter solstice in the Northern Hemisphere. Thus, it is expected that the potential of plume detection could increase if acquisitions around the summer solstice and Northern Hemisphere were considered (e.g., due to better SNR and lower shadowing).
In summary, the unique configuration of the WV-3 mission can substantially benefit current mapping efforts with a positive impact on the definition of a future methane observing system as proposed by recent EU regulations (European Commision, 2020). Very high resolution satellite observations of methane point sources as from WV-3 could play an integral role in future near-real-time emission detection service.
The data are available from the author upon request.
ESG, JG, IIL, and LG contributed to the conceptualization of the study. JG implemented the source retrieval algorithms and methane plume simulations. ESG produced the sensitivity analysis and site studies. DJV produced large eddy simulations and supported the quantification of the methane emissions. ESG and JG wrote the original draft, and all authors reviewed and edited the manuscript.
The contact author has declared that neither they nor their co-authors have any competing interests.
Publisher's note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
First, we would like to thank the European Space Agency and European Space Imaging for the access to the WV-3 data through the Third-Party Missions scheme. We personally thank Silvester Fischer and Thierry Buettel from European Space Imaging for their assistance in the product details and processing. We thank Daniel Cusworth (JPL) for the access to realistic methane plume simulations with WRF-LES. Last but not least, we thank the referees, Vladimir Savastiouk and Folkert Boersma, for their useful comments.
This research has been supported by the ESA (contract no. 4000134929) and the ESA Living Planet Fellowship (ESA contract no. 4000130980/20/I-NS).
This paper was edited by Alexander Kokhanovsky and reviewed by Vladimir Savastiouk, Folkert Boersma, and one anonymous referee.
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