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Atmospheric Measurement Techniques An interactive open-access journal of the European Geosciences Union
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AMT | Articles | Volume 12, issue 1
Atmos. Meas. Tech., 12, 735-747, 2019
© Author(s) 2019. This work is distributed under
the Creative Commons Attribution 4.0 License.
Atmos. Meas. Tech., 12, 735-747, 2019
© Author(s) 2019. This work is distributed under
the Creative Commons Attribution 4.0 License.

Research article 01 Feb 2019

Research article | 01 Feb 2019

Towards imaging of atmospheric trace gases using Fabry–Pérot interferometer correlation spectroscopy in the UV and visible spectral range

Fabry–Pérot interferometer correlation spectroscopy of atmospheric trace gases
Jonas Kuhn1,2, Ulrich Platt1,2, Nicole Bobrowski1,2, and Thomas Wagner2 Jonas Kuhn et al.
  • 1Institute of Environmental Physics, University of Heidelberg, Heidelberg, Germany
  • 2Max Planck Institute for Chemistry, Mainz, Germany
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Many processes in the lower atmosphere including transport, turbulent mixing and chemical conversions happen on timescales of the order of seconds (e.g. at point sources). Remote sensing of atmospheric trace gases in the UV and visible spectral range (UV–Vis) commonly uses dispersive spectroscopy (e.g. differential optical absorption spectroscopy, DOAS). The recorded spectra allow for the direct identification, separation and quantification of narrow-band absorption of trace gases. However, these techniques are typically limited to a single viewing direction and limited by the light throughput of the spectrometer set-up. While two-dimensional imaging is possible by spatial scanning, the temporal resolution remains poor (often several minutes per image). Therefore, processes on timescales of seconds cannot be directly resolved by state-of-the-art dispersive methods.

We investigate the application of Fabry–Pérot interferometers (FPIs) for the optical remote sensing of atmospheric trace gases in the UV–Vis spectral range. By choosing a FPI transmission spectrum, which is optimised to correlate with narrow-band (ideally periodic) absorption structures of the target trace gas, column densities of the trace gas can be determined with a sensitivity and selectivity comparable to dispersive spectroscopy, using only a small number of spectral channels (FPI tuning settings). Different from dispersive optical elements, the FPI can be implemented in full-frame imaging set-ups (cameras), which can reach high spatio-temporal resolution. In principle, FPI correlation spectroscopy can be applied for any trace gas with distinct absorption structures in the UV–Vis range.

We present calculations for the application of FPI correlation spectroscopy to SO2, BrO and NO2 for exemplary measurement scenarios. In addition to high sensitivity and selectivity we find that the spatio temporal resolution of FPI correlation spectroscopy can be more than 2 orders of magnitude higher than state-of-the-art DOAS measurements. As proof of concept we built a 1-pixel prototype implementing the technique for SO2 in the UV. Good agreement with our calculations and conventional measurement techniques is demonstrated and no cross sensitivities to other trace gases are observed.

1 Introduction
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Within the last decades, progress in optical remote sensing of atmospheric trace gases has led to a better understanding of many important processes including air pollution, ozone, and halogen chemistry and the evolution of volcanic plumes. Narrow-band structures in the trace gas molecule's absorption spectrum are used to identify and quantify the amount of a trace gas integrated along a line of sight, i.e. its column density (CD, typically in units of molecules per cubic centimetre), and to separate its absorption signal from interfering gas absorptions and scattering processes.

Differential optical absorption spectroscopy (DOAS; see Platt and Stutz2008, for details) has become a well established technique for atmospheric trace gas remote sensing in the UV–Vis with high sensitivity (detection limits within the parts per billion to parts per trillion range for atmospheric light paths of a few kilometres). A spectrometer and a telescope with narrow field of view (FOV) are used to record spectra I(λ) of scattered sunlight, which are compared to a reference spectrum I0(λ). The Beer–Lambert law describes the corresponding spectral optical density τ(λ) with σi(λ) and ci(l) being the absorption cross section and the concentration of trace gas species i along a line of sight L, respectively:


Atmospheric UV–Vis optical densities are dominated by trace gas absorption and scattering processes at air molecules or aerosols. The known absorption cross sections of the trace gases together with a polynomial, which accounts for the broad-band absorption and scattering effects, are fitted to the measured spectral optical density. The fit coefficients represent the CDs Si=0Lci(l)dl, i.e. the integrated trace gas concentration along the light path difference of I(λ) and the reference I0(λ). In principle, spatial distributions of trace gases (images or height profiles) can be recorded by scanning of viewing angles with a narrow FOV telescope (e.g. multi-axis DOAS; Hönninger et al.2004). More complicated optical set-ups allow us to record spectra of an entire image column at once by using a two-dimensional detector array (e.g. imaging DOAS; Lohberger et al.2004). Images can then be recorded by column (push broom) scanning. The acquisition times of these techniques used to be rather large (often several minutes per image or profile for typical trace gas CDs), limiting their application to processes that are spatially homogeneous on that timescale or processes with very high trace gas CDs. Recently, Manago et al. (2018) reported NO2 measurements with a hyperspectral camera based on the imaging DOAS technique with considerably higher temporal resolution (∼0.08 Hz).

Determination of two-dimensional atmospheric trace gas distributions with high time resolution at timescales of the order of seconds, i.e. fast imaging, of atmospheric trace gases is possible with techniques recording all spatial pixels of an image at once for a low number of spectral channels (see e.g. Platt et al.2015). This allows the study of phenomena which are not accessible to conventional scanning methods. With fast trace gas imaging techniques, sources and sinks of trace gases can be identified and quantified on much smaller spatial and temporal scales than with conventional remote-sensing techniques. This allows us to, for instance, gain insight into small-scale mixing processes and to distinguish chemical conversions from transport.

Most of the presently used atmospheric trace gas imaging schemes use either a set of two band pass filters (BPFs) (e.g. SO2 camera, ∼1 Hz for volcanic emissions; see e.g. Mori and Burton2006; Bluth et al.2007; Kern et al.2010; Platt et al.2018) or a tuneable BPF as a wavelength selective element (e.g. NO2 camera, ∼3 min per image for stack emissions of power plants; Dekemper et al.2016). These techniques either involve intricate optical set-ups with low light throughput or yield a rather coarse spectral resolution, which might result in strong cross interferences (see e.g. Lübcke et al.2013; Kuhn et al.2014).

Here we study the application of Fabry–Pérot interferometers (FPIs) as wavelength selective elements for trace gas imaging in the UV–Vis range. The periodic FPI transmission spectrum is matched to the spectral absorption structures of trace gases that often show a similar periodicity. Thanks to the high correlation of the transmission spectrum of the wavelength selective element and the trace gas absorption spectrum, a high sensitivity can be reached and cross interferences with other absorbers are minimised, even if only a small number of spectral channels (FPI tuning settings) is used (see Kuhn et al.2014,  and the discussion in Sect. 3.2 below). Air spaced FPI etalons are very robust devices and allow for simple optical designs that can easily be implemented in imaging sensors. We present a model study on the sensitivity and selectivity of FPI correlation spectroscopy applied to SO2, BrO and NO2 (Sect. 3). For exemplary measurement scenarios, we infer the possible spatio-temporal resolution of these measurements for a specific instrument implementation. We find that, for the three gases, imaging with spatio-temporal resolutions about 2 orders of magnitude higher than state-of-the-art methods should be possible. In addition, we present a proof-of-concept study of the technique for volcanic sulfur dioxide (SO2), validating the expected high accuracy and sensitivity of the technique with a 1-pixel prototype instrument. Further, we show that SO2 CDs can be accurately retrieved from the recorded data without calibration (Sect. 4).

Figure 1(a) FPI schematics indicating the splitting of incident radiation into partial beams that interfere to cause the FPI transmittance spectrum (b), which is characterised by periodic transmission maxima with a FWHM of δλ and a FSR of Δλ. The BrO absorption cross section (upper panel) shows approximately periodic structures allowing for a high correlation with spectral FPI transmittance. This leads to a modulation of the BrO optical density as seen through the FPI with changing surface displacement d (c). The apparent absorbance is the difference of the optical densities of FPI settings A and B, representing maximum and minimum correlation of FPI transmission and absorption cross section σ.


2 Fabry–Pérot interferometer correlation spectroscopy
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2.1 Fabry–Pérot interferometer

The FPI is a fundamentally very simple optical device, known for more than a century (e.g.  Perot and Fabry1899). In principle, it consists of two plane parallel surfaces each with reflectance R, separated by a distance d (see Fig. 1). The medium between the plates has the index of refraction n. Incident light (angle of incidence α) is split up in partial beams with different optical path lengths between the two surfaces. Due to interference of the transmitted partial beams, the spectral transmission of the FPI is characterised by periodic transmission peaks, referring to constructive interference. For high enough orders of interference, the free spectral range (FSR) Δλ between two transmission peaks in units of wavelength λ is approximately given by


The finesse F of a FPI represents the ratio of FSR to the full width half maximum (FWHM) δλ of a transmission peak:


The finesse is a measure for the number of effectively interfering partial beams and therefore increasing with the surface reflectance. However, it also depends on the alignment and quality of the surfaces.

The spectral transmission as a function of λ and the FPI's instrument parameters is given by


Despite its simple design, the challenge in manufacturing FPI devices lies in creating set-ups keeping d stable to a fraction of a wavelength across the effective aperture.

Table 1Differential CDs assumed for the different measurement scenarios. The values represent high values for CD variations within a typical imaging FOV. The targeted detection limits are indicated in italic.

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2.2 Detection principle

The concept of using FPI correlation to detect atmospheric trace gases is described in Kuhn et al. (2014). The correlation of periodic absorption structures of atmospheric trace gases and the FPI transmission is exploited. An apparent absorbance τ̃i of a trace gas i is calculated from the optical densities of an on-band τA and off-band τB channel:


Si denotes the CD of a trace gas i. For the on-band channel, the spectral pattern of the FPI transmittance is chosen to correlate with the absorption band structure of the target trace gas, while for the off-band channel the FPI is tuned to show minimum correlation with the target trace gas absorption (see Fig. 1). The apparent absorbance is – for low trace gas optical densities – proportional to the CD of the trace gas. The proportionality is Δσ, representing the difference of the effective absorption cross section seen by channel A and channel B. The optical densities τk are calculated from measured radiances Ik transmitted by the FPI in a setting k=A,B:


Ik, 0 denotes the reference radiance without the target trace gas in the light path. In practice, a wavelength range Δλ of high correlation of spectral trace gas absorption and FPI transmission is preselected with a BPF. Within this spectral range the FPI physical parameters are optimised. Figure 1c shows the optical density of BrO seen through an FPI with varying surface displacement d. The maximum difference between maximum and minimum optical density determines the FPI settings A and B. In addition, the finesse is chosen to maximise the signal-to-noise ratio.

Here we apply FPI correlation spectroscopy for passive imaging of a trace gas in the atmosphere. This means that the light source is scattered sky radiation that is measured within an imaging FOV (e.g. 20 aperture angle). We assume in the following that a reference I0 (i.e. a part without trace gas) is always present within the image, so that S denotes the differential trace gas CD compared to that reference.

The proportionality Δσ of apparent absorbance τ̃ and trace gas CD S (see Eq. 5) can be calculated from literature absorption cross sections of the target trace gas, a background spectrum I0(λ) and a modelled instrument transfer function (see Sects. 3.1 and 4.2). Alternatively, Δσ can be determined through calibration (see e.g. Lübcke et al.2013; Sihler et al.2017).

3 Model study for SO2, NO2 and BrO
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FPI correlation spectroscopy can be applied to every trace gas species that yields sufficiently strong spectral absorption structures in the regarded wavelength range. In this section we present exemplary model studies for imaging of SO2, NO2 and BrO. For each target trace gas we regard a typical exemplary measurement scenario (Table 1). For the target species BrO and SO2 we use typical measurement scenarios of volcanic emissions in the UV spectral range. For SO2 we assume CDs that are typically measured in volcanic plumes of a comparably weak volcanic emitter or an already highly diluted plume (required detection limit of 1×1017molec cm−2; see Table 1). We additionally chose a high and probably disturbing NO2 CD (1×1017molec cm−2) in order to make the scenario also applicable to SO2 measurements at ship or industrial stack emissions. Existing filter-based SO2 cameras are subject to strong cross interferences in this CD range (see e.g. Lübcke et al.2013; Kuhn et al.2014). In the scenario for BrO we assume a relatively strong but not uncommon volcanic emitter, with BrO mixing ratios of tens to hundreds of parts per trillion within the plume (required detection limit of 1×1014molec cm−2; see Table 1) and high SO2 CDs (3×1018molec cm−2). Gradients in the BrO distributions can give insight into in-plume halogen chemistry (see e.g. Bobrowski et al.2007; von Glasow2010; Roberts et al.2014). The NO2 scenario (blue spectral range) is applicable to measurements of stack emissions at, for example, a coal power plant (see e.g. Dekemper et al.2016) but also to local gradients induced by traffic (required detection limit of 1×1016molec cm−2; see Table 1).

We calculate the sensitivities and study the cross interference of the apparent absorbance with other atmospheric absorbers for typical differential CDs for the respective measurement scenario. Table 1 lists the assumed differential CDs of the trace gases absorbing in the same spectral range as the trace gases under investigation. For these potentially interfering trace gases we chose relatively high values, so that the indicated cross interferences correspond to upper limits. The listed CDs represent differential CDs across a typical image FOV (∼20), assuming that within the image a reference region I0 without the target trace gas is always present.

In a second step, we calculate the corresponding photon budgets in order to infer the approximate achievable spatial and temporal resolution of the respective imaging measurement.

3.1 Description of the model

The apparent absorbance is calculated from radiances Ik (in photonss-1mm-2sr-1) of scattered solar radiation transmitted by the respective spectral channel k=A,B (on-band and off-band FPI setting):


A spectrum recorded on a clear day in Heidelberg with a solar zenith angle of 73 (160 relative solar azimuth, 89 viewing zenith angle) was used to approximate the spectral radiance I0(λ). I0(λ) was scaled with scattered sky radiance measurements from Blumthaler et al. (1996). The radiance measurements were performed in Innsbruck in February 1995 with a solar zenith angle of 68. For our calculations we used the values for a 180 relative solar azimuth and 70 viewing zenith angle. Si is the CD of an absorbing gas species i with spectral absorption cross section σi(λ). TFPI, k is the FPI transmittance in configuration k (see Eq. 4) and TBPF the transmittance of the BPF isolating the measurement wavelength range for the respective target trace gas. TBPF was modelled with a higher-order Gaussian function:


with a FWHM of


P describes the peak transmission at a central wavelength λBPF. An order p=6 was used to approximate interference filter transmission profiles.

With Eq. (5) and the intensities Ik from Eq. (7), the apparent absorbance τ̃i can be calculated, allowing us to study the sensitivity and selectivity of the detection of a trace gas i for given FPI instrument settings.

Table 2Instrument parameters of FPI, BPF and optical set-up used for the simulations. The radiance for the on-band setting IA at the detector was approximated based on the instrument parameters and sky radiance values from Blumthaler et al. (1996).

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In addition, we approximate the respective detection limits based on photon shot noise. In order to calculate the number of photons that reach the detector of the imaging device, we need to know the etendue (product of entrance area A and aperture solid angle Ω) of the employed optics. Kuhn et al. (2014) suggest several optical set-ups for FPI correlation spectroscopy imaging implementations. Here, we chose the set-up in which, with help of image space telecentric optics (see Fig. 5), the incident radiation from the imaging FOV is parallelised before traversing the FPI and BPF. In order to avoid strong blurring of the FPI transmission spectrum due to different incidence angles, the divergence Θ of the light beams traversing the FPI should not be much larger than Θ=1. With a lens of focal length f this condition limits the maximum aperture radius a to


The FPI clear aperture radius aFPI determines the imaging FOV aperture angle:


The etendue per pixel Epix is determined by the spatial resolution of the recorded image, which can be varied by binning individual pixels. For npix being the number of pixels along a column of a square detector array, the approximate etendue per pixel of the instrument is


The detectors' quantum efficiency and losses within the optics are considered to be not wavelength dependent in the regarded spectral ranges and combined in a loss factor η. We chose a somewhat lower loss factor for the UV range (0.25 for SO2 and BrO) compared to the visible range (0.5 for NO2) due to the higher quantum efficiency of commonly used detectors. Each FPI channel (on-band and off-band setting) requires one image acquisition. We assume a measurement limited by photoelectron shot noise, where for an exposure time Δt the number of counted photoelectrons per pixel and image is


with an uncertainty of ΔNphe,pix=Nphe,pix. The uncertainty in the apparent absorbance τ̃ is then


assuming the intensities Ik for the two FPI settings k=A,B are similar and that the reference intensities I0, k have to be recorded only once.

Note that the used sky radiances, loss factors and dimensions of the optics (see Table 2) represent conservative assumptions. For instance the light throughput could be enhanced by more than an order of magnitude by choosing a different optical set-up (see Kuhn et al.2014). There, the FPI is placed in front of the lens using the full clear aperture and the full aperture angle of the FPI and the optics. Each viewing direction of the FOV, however, will have a different incidence angle onto the FPI and therefore a different FPI transmission spectrum, which has to be accounted for in the data analysis. Alternatively, simply a larger FPI could be used. The results of the following calculations for the image space telecentric optics, therefore, represent lower limits of the performance.

Figure 2Model results for SO2: (a) the differential optical densities of the assumed differential trace gas CDs are plotted in the upper panel. The lower panel shows the spectral radiance of the sky (dashed line) and the transmitted spectral radiances of the FPI and BPF (drawn lines, on-band in black, off-band in grey). Panel (b) shows the calculated calibration curve for SO2 only (drawn line) and with different interfering species included (dashed lines, CDs in molecules per square centimetre; see legend and Table 1).


Figure 3Model results for BrO: (a) the differential optical densities of the assumed differential trace gas CDs are plotted in the upper panel. The lower panel shows the spectral radiance of the sky (dashed line) and the transmitted spectral radiances of the FPI and BPF (drawn lines, on-band in black, off-band in grey). Panel (b) shows the calculated calibration curve for BrO only (drawn line) and with different interfering species included (dashed lines, CDs in molecules per square centimetre; see legend and Table 1).


Figure 4Model results for NO2: (a) the differential optical densities of the assumed differential trace gas CDs are plotted in the upper panel. The lower panel shows the spectral radiance of the sky (dashed line) and the transmitted spectral radiances of the FPI and BPF (drawn lines, on-band in black, off-band in grey). Panel (b) shows the calculated calibration curve for NO2 only (drawn line) and with different interfering species included (dashed lines, CDs in molecules per square centimetre; see legend and Table 1).


3.2 Results of the simulations

The FPI correlation spectroscopy technique allows for numerous different realisations regarding the used spectral window and FPI instrument parameters that can be chosen according to, for example, measurement conditions or availability of optical components (FPI, BPF). Here, we identified spectral windows in which the target trace gas absorption cross sections exhibit approximately periodic structures and appropriate FPI parameters were determined in order to maximise the correlation of FPI transmission and trace gas absorption according to the procedures described in Kuhn et al. (2014). Table 2 lists the parameters for the exemplary set-ups we use in this work.

The results for SO2, BrO and NO2 are summarised in Figs. 2, 3 and 4, which show the differential optical densities of the target trace gas and the potentially interfering trace gases for the respective measurement wavelength ranges (Figs. 2a, 3a, 4a). In the lower panels, the transmitted spectral radiances of the respective FPI spectral channels (on-band, off-band) are plotted. The SO2 and NO2 trace gas optical densities clearly dominate the total differential optical density for the targeted detection limits. For BrO the other trace gases exhibit differential optical depths on the same order of magnitude as BrO. In Figs. 2b, 3b and 4b, the respective simulated calibration curves are plotted, where the dashed lines indicate the impact of the individual interfering gases for the assumed amounts. For all three gases these impacts are well below the targeted detection limit. Especially for the case of BrO this illustrates how FPI correlation spectroscopy can effectively separate the absorption structure of a single trace gas from a multitude of trace gas optical densities of the same order of magnitude. By using more than two FPI settings, the selectivity can be enhanced even further.

Figure 5Image space telecentric optical set-up for parallelising light from the imaging FOV before traversing the FPI and BPF.


Table 3Simulation results: the spatial resolution of a FPI correlation spectroscopy measurement was calculated for an exposure time of 10 s and the target detection limits, shown in Table 1.

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The absorption bands of NO2 are not ideally periodic in the chosen wavelength window. Therefore, at first glance they appear to be non-ideal for FPI correlation. The apparent absorbance, however, is still reasonably high with extremely low cross interferences to water vapour and O4. This demonstrates that periodical absorption structures are ideal but not necessary for FPI correlation spectroscopy. For a different measurement scenario (here we optimised for stack and ship emissions; see above) there might also be a better choice for instrument parameters. For instance for a high-radiance and low-NO2 scenario one might use a single FPI transmission peak on the NO2 absorption band at ∼435 nm (as setting A) and at ∼438 nm (as setting B) in order to increase the sensitivity (see Fig. 4).

Table 3 summarises the results of the photon budget calculations. We calculated the maximum possible spatial resolution of the imaging measurement for a 10 s exposure time and the instrument parameters listed in Table 2. For this, spatial pixels are co-added until the targeted detection limit was reached. We find that for the targeted detection limits the spatial resolutions of the imaging measurements for the chosen parameters are 226 by 226 pixels for SO2, 51 by 51 pixels for BrO and 252 by 252 pixels for NO2 for a temporal resolution of 10 s. The temporal resolution could be enhanced at the expense of the spatial resolution or vice versa. For instance, cutting the linear spatial resolution in half (e.g. from 226 by 226 to 113 by 113 pixels for SO2), would reduce the temporal resolution to 5 s for the same detection limit.

When comparing to corresponding DOAS measurements the increase in spatio-temporal resolution becomes evident. A state-of-the-art DOAS measurement takes around 1 s to reach a detection limit of 1×1014moleccm-2 BrO for one spatial pixel. To scan the ca. 2600 pixels of the assumed BrO image would take 2600 s. This is, however, a comparison with an instrument that is not optimised for these kinds of imaging measurements. Manago et al. (2018) recently recorded NO2 images with a hyperspectral camera, based on imaging DOAS. A detection limit of around 1×1016moleccm-2 NO2 is reached with a spatial resolution of 480 by 640 pixels and 3 by 3 pixel binning with 12 s frame−1. This is only a factor of 2.2 slower than our calculation for the telecentric set-up. By applying the standard optics introduced in Kuhn et al. (2014), the light throughput is increased by another factor of 32. Therefore, theoretically, the FPI technique can be a factor of ∼70 times faster. Of course these values always depend on the size of the assumed instrument optics. Our results show that FPI correlation spectroscopy can be about 2 orders of magnitude faster than conventional DOAS measurements while maintaining a similar degree of selectivity and interference suppression.

The presented results of the exemplary calculations for SO2, BrO and NO2 suggest that FPI correlation spectroscopy can also be implemented for other trace gases with similarly strong and structured absorption, such as, for example, O3, HCHO, IO or OClO.

4 Proof of concept: field measurements of volcanic SO2
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4.1 Sensitivity and ozone interference

The above model study on trace gas detection with FPI correlation spectroscopy was validated in a proof-of-concept field study for volcanic SO2. In a 1-pixel prototype a single photodiode was used as a detector. A BPF (λBPF310nm,δλ,BPF10nm) was used for the preselection of a wavelength range, for which the SO2 differential absorption is strong and approximately periodic (see Fig. 2). A FPI (air-spaced etalon from SLS Optics Ltd.) with a FSR of 2.1 nm and a finesse of 7 across a clear aperture of 20 mm was tilted by a servomotor in order to tune it to the on-band and off-band transmission settings. The individual plates of the FPI have a finite thickness and two surfaces; the outer surfaces have an anti-reflective coating and are slightly wedged from the inner surfaces of the plates, so their influence can be neglected here. The optical set-up behind FPI and BPF consists of a fused silica lens (f≈50 mm), which projects light from a narrow FOV (∼0.8 aperture angle) onto the photodiode.

Radiances for the on-band and off-band channels were recorded, delivering an apparent absorbance measurement with 0.42 Hz. A telescope (∼0.5 aperture angle) was co-aligned with the 1-pixel FPI set-up and connected to a temperature-stabilised spectrometer (spectral resolution ∼0.8 nm). The recorded spectra (∼0.13 Hz) were evaluated with the DOAS algorithm.

The measurement was performed at the Osservatorio Vulcanologico Pizzi Deneri (lat 37.766, long 15.017, 2800ma.s.l.) at Mt Etna on Sicily on 30 July 2017. The device was pointed towards the volcanic plume of Mt Etna with a constant viewing angle (8 viewing elevation, azimuth 280 N). A plume-free part of the sky (zenith viewing direction) was used for reference measurements and recorded prior to the plume measurement. Figure 6 shows the time series of the apparent absorbance of the FPI correlation spectroscopy prototype together with the SO2 CD retrieved from the co-recorded spectra. The apparent absorbance shows high correlation with the retrieved SO2 CD. In Fig. 7 the correlation plot is shown. For high SO2 CDs the sensitivity of τ̃SO2 decreases slightly due to saturation effects. The scatter of the values mainly originates from slight misalignment and the difference of the two narrow FOVs.

Figure 6Time series of the apparent absorbance of the 1-pixel FPI correlation spectroscopy prototype for SO2 detection (top trace, left scale) recorded at Etna, Sicily, on 30 July 2017. A co-aligned telescope was used to simultaneously record spectra for DOAS evaluation of SO2 and O3 (centre and bottom traces and right and bottom left scales, respectively). The apparent absorbance nicely correlates with the SO2 CD (see Fig. 7), while no O3 impact is observable. The growth of the retrieved O3 differential CD is expected due to the increasing stratospheric O3 column for increasing solar zenith angle (see text).


Figure 7Correlation plot of the recorded FPI correlation spectroscopy apparent absorbance and the SO2 CD retrieved by DOAS. A sensitivity of about ΔσSO2 of 10−19 cm2 is reached for lower SO2 CDs. For higher CDs a flattening of the curve is observed that is induced by saturation effects due to the high SO2 optical densities at the absorption peaks.


The recorded UV spectra also allow for evaluation of the O3 absorption. The lower panel of Fig. 6c shows the change of the differential O3 CD during the measurement with respect to the reference. The observed increase in the O3 CD by more than 4×1018moleccm-2 during the plume measurement is due to the increasing stratospheric light path with increasing solar zenith angle (63.58 to 79.31 during the measurement sequence). Within an imaging FOV (of 17, for example) much lower differential O3 CDs are expected (see Table 2), since all pixels are similarly affected by the change in O3 background. Even with this extreme change in O3 CD no impact on the recorded SO2 apparent absorbances is observed.

The presented data also indicate the potential of using an additional DOAS measurement for the calibration of the apparent absorbance of an FPI imaging device. The position of the narrow FOV of a DOAS telescope pointing into the wide imaging FOV can be retrieved from time series and used for an in-operation calibration (see e.g. Lübcke et al.2013; Sihler et al.2017).

4.2 Calculation of SO2 CDs by modelling effective absorption cross sections

As stated in Sect 2.2 we can also directly calculate the SO2 CDs from the apparent absorbance τ̃ by modelling the effective absorption cross sections and thereby ΔσSO2. This requires knowledge about the instrument spectral transmission, the background scattered light spectrum and the SO2 absorption cross section.

We modelled the instrument transfer function with the transmission spectrum of the used BPF, the calculated FPI transmission spectrum (see Sect. 3.1) and the quantum efficiency of the photodiode. The background scattered sunlight spectrum was modelled using a high-resolution solar atlas spectrum according to Chance and Kurucz (2010), scaled by the wavelength to the fourth power (assuming Rayleigh scattering) and multiplied with the transmission of the total slant atmospheric ozone column. The ozone column was estimated to 2.5×1019moleccm-2 using the vertical ozone column (for the measurement day according to satellite measurements, TEMIS database; Veefkind et al.2006) multiplied with a geometric air mass factor for the average solar zenith angle during the measurement. The SO2 absorption cross section of Vandaele et al. (2009) was used.

Figure 8Correlation plot of the SO2 CDs retrieved by modelling and the SO2 CDs retrieved by DOAS. The error bars indicate the uncertainty of the FPI finesse (±3 %) and the background spectral radiance in the model (±10 %) and the DOAS retrieval error. A high correlation is observed and the saturation effect is accounted for by the model as well.


The largest uncertainties are the finesse of the FPI and the modelled background spectrum, in which Rayleigh scattering approximation and the assumed ozone column introduce uncertainties. A finesse of about 7 is reported by the manufacturer for perpendicularly incident radiation. For the instrument model we have to calculate the effective finesse for a divergent light ray (∼0.8 aperture angle) for the two FPI tilt positions (around 0 for setting B and 5 for setting A, corresponding to a finesse of around 7 and 5, respectively). Since the divergent light ray reaching the detector is dependent on focal length, detector area and the alignment of the optical components and due to the uncertainty in the reflectance of the FPI, we can determine the finesse only with an uncertainty of ±3 %. Further, we estimate an uncertainty in the background spectrum by ±10 % in our calculation, accounting for uncertainties in atmospheric radiative transfer and ozone column.

Figure 8 shows the SO2 CDs calculated with the described FPI model as a function of the SO2 CDs retrieved from the DOAS spectra. We observe an excellent agreement with a slope of 0.99, an intercept of 7.5×1015moleccm-2 and R2=0.96. The uncertainties in background spectral radiance and finesse result in a uncertainty in the SO2 sensitivity ΔσSO2 of around ±10 % and therefore a relative uncertainty of ±10 % in the retrieved SO2 CD. Here, it is important to highlight the difference between ozone interference with the apparent absorbance and the influence of an uncertainty in the total ozone column assumed in the model. The former seems to be negligible as shown by the measurements (Fig. 6) and in the model study (Sect. 3.2). The latter influences the modelled sensitivity of the measurement. This means it introduces a small relative uncertainty to the retrieved CDs, which has almost no influence on the detection limit. The saturation effects observed for high CDs in the apparent absorbances (see Fig. 7), meaning the CD dependency of ΔσSO2, are accounted for by the model as well. This is a very promising result, pointing towards the possibility of calibration-free measurements, which would be another major advantage of the FPI correlation spectroscopy compared to, for example, filter-based SO2 cameras.

4.3 Imaging

The 1-pixel FPI correlation spectroscopy prototype, introduced in this study, can be implemented in a full-frame imaging instrument. This is the major advantage of the technique compared with the DOAS technique. The imaging implementation can be achieved with, for example, the image space telecentric optical set-up, used for the above calculations and shown in Fig. 5. In principle, the single-pixel detector (photodiode) is replaced by a two-dimensional detector array (UV sensitive for SO2 and BrO) and an aperture stop is added in the focal plane in front of the lens. This would, however, reduce the light throughput per pixel of the imaging set-up compared to the 1-pixel prototype. Alternatively, the FPI could be placed in front of the lens using the full clear aperture and the full aperture angle of the FPI and the optics, increasing the light throughput by a factor of 32 (see Kuhn et al.2014). This leads to a much higher light throughput; however, the incidence angle of the incident light onto the FPI and thereby the FPI transmission spectrum becomes dependent on the pixel (i.e. the viewing direction within the imaging FOV) and has to be accounted for in the data evaluation.

5 Conclusions
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Many locally variable atmospheric processes are difficult to quantify with state-of-the-art UV–Vis remote-sensing methods (e.g. DOAS) due to the limited spatio-temporal resolution. This makes it difficult to, for example, study the emission of point sources or to separate the effects of transport and chemical conversion on local scales. Kuhn et al. (2014) proposed the FPI correlation spectroscopy for SO2 in the UV wavelength range after similar approaches have been studied in infrared wavelength ranges (e.g.  Wilson et al.2007; Vargas-Rodríguez and Rutt2009). The major motivation is to reduce the number of spectral channels used for the trace gas detection in order to increase the spatio-temporal resolution of the measurement while maintaining its selectivity.

In a model study we investigated the sensitivity and determined the photon budget of FPI correlation spectroscopy for three measurement scenarios for SO2, BrO and NO2. For SO2 we assumed a scenario with rather low volcanic emissions, which is also representative for industrial stack or ship emissions. For BrO a scenario with stronger volcanic emissions was assumed, with BrO mixing ratios of 10 to 100 ppt within the volcanic plume and high SO2 CDs. The NO2 measurement scenario represents typical stack emissions of power plants and gradients of local air pollution induced by traffic, for example.

For all three investigated gases, cross interferences with other trace gases absorbing in the preselected spectral ranges were found to be very low, meaning that the selectivity of FPI correlation spectroscopy can be similar to the selectivity of conventional techniques (e.g. DOAS). In this study, we only used two FPI settings. A larger number of FPI settings could be used to further reduce possible cross interferences.

Using rather conservative assumptions regarding the intensity of the incoming radiation and the size of the instrument optics, we calculated the highest possible spatio-temporal resolution of the FPI correlation spectroscopy measurements for the different scenarios and found that they can be more than 2 orders of magnitude higher compared to state-of-the-art DOAS measurements for the same trace gas CD. This means that in the same time period a conventional dispersive technique records a single viewing direction (i.e. a single spatial pixel), almost an entire image can be recorded with the FPI correlation spectroscopy. This strongly indicates that future instruments based on FPI correlation spectroscopy can provide unprecedented insight into short time or small-scale processes in the atmosphere.

In the second part, we presented a proof-of-concept field study for FPI correlation spectroscopy applied to volcanic SO2, which confirms the model simulations by comparing the measured apparent absorbance to SO2 CDs retrieved by a co-aligned DOAS measurement. One particularly important finding is that, as expected from the model study, no O3 cross interference can be observed over a large O3 CD range. Further, SO2 CDs could be directly calculated from the instrument model and a very simple radiative transfer model very accurately and with a ∼10 % uncertainty of the sensitivity. This indicates that CDs can be retrieved directly from the FPI radiance data without calibration.

The extension of the 1-pixel prototype to a camera can be accomplished comparably easily by minor modifications of the optics and by using a UV-sensitive detector array and should be the aim of future studies. By replacing the FPI and the BPF, the instrument is adjusted to measure different trace gases, e.g. BrO and NO2, according to the model calculations performed in Sect. 3.

The applications of UV–Vis FPI correlation spectroscopy mentioned in this work represent only some examples for trace gases and phenomena that could be studied. Beyond the volcanological application, FPI imaging can for instance be used to study SO2 in air pollution or BrO in salt pans (see e.g. Holla et al.2015). The technique can also be applied to other trace gases with similarly strong and structured absorption, such as, for example, O3, HCHO, IO or OClO.

Data availability
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Data availability. 

The data used for the proof-of-concept study can be obtained from the authors upon request.

Author contributions
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Author contributions. 

All authors contributed to the conception and design of the study and substantially worked on several rounds of paper extension and revision. NB helped with the field measurements. JK developed the model, designed and built the instrument, performed and evaluated the measurements, and wrote the draft of the paper.

Competing interests
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Competing interests. 

The authors declare that they have no conflict of interest.

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We would like to thank SLS Optics Ltd. for sharing their expertise in designing and manufacturing etalons. We also thank Jan-Lukas Tirpitz and Denis Pöhler for their help with instrument design and electronics. We gratefully acknowledge financial support from the Deutsche Forschungsgemeinschaft (project DFG PL 193/23-1) and the Heidelberg Graduate School of Fundamental Physics.

The article processing charges for this open-access
publication were covered by the Max Planck Society.

Edited by: Andreas Hofzumahaus
Reviewed by: Emmanuel Dekemper and one anonymous referee

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Publications Copernicus
Short summary
We study a novel remote-sensing technique for atmospheric trace gases absorbing in the UV and visible spectral range. Using Fabry–Perot interferometers with a spectral transmission matched to the trace gas's spectral absorption allows for imaging trace gases with high sensitivity and selectivity. The thereby achieved high spatio-temporal resolution enables the study of small-scale and dynamic processes in the atmosphere. We present sample calculations and a proof-of-concept study.
We study a novel remote-sensing technique for atmospheric trace gases absorbing in the UV and...