the Creative Commons Attribution 4.0 License.

the Creative Commons Attribution 4.0 License.

# Linearization of the effect of slit function changes for improving Ozone Monitoring Instrument ozone profile retrievals

### Xiong Liu

### Kelly Chance

### Jae-Hwan Kim

We introduce a method that accounts for errors caused by the slit function in an optimal-estimation-based spectral fitting process to improve ozone profile retrievals from the Ozone Monitoring Instrument (OMI) ultraviolet measurements (270–330 nm). Previously, a slit function was parameterized as a standard Gaussian by fitting the full width at half maximum (FWHM) of the slit function from climatological OMI solar irradiances. This cannot account for the temporal variation in slit function in irradiance, the intra-orbit changes due to thermally induced change and scene inhomogeneity, and potential differences in the slit functions of irradiance and radiance measurements. As a result, radiance simulation errors may be induced due to convolving reference spectra with incorrect slit functions. To better represent the shape of the slit functions, we implement a more generic super Gaussian slit function with two free parameters (slit width and shape factor); it becomes standard Gaussian when the shape factor is fixed to be 2. The effects of errors in slit function parameters on radiance spectra, referred to as pseudo absorbers (PAs), are linearized by convolving high-resolution cross sections or simulated radiances with the partial derivatives of the slit function with respect to the slit parameters. The PAs are included in the spectral fitting scaled by fitting coefficients that are iteratively adjusted as elements of the state vector along with ozone and other fitting parameters. The fitting coefficients vary with cross-track and along-track pixels and show sensitivity to heterogeneous scenes. The PA spectrum is quite similar in the Hartley band below 310 nm for both standard and super Gaussians, but is more distinctly structured in the Huggins band above 310 nm with the use of super Gaussian slit functions. Finally, we demonstrate that some spikes of fitting residuals are slightly smoothed by accounting for the slit function errors. Comparisons with ozonesondes demonstrate noticeable improvements when using PAs for both standard and super Gaussians, especially for reducing the systematic biases in the tropics and midlatitudes (mean biases of tropospheric column ozone reduced from $-\mathrm{1.4}\sim \mathrm{0.7}$ to 0.0∼0.4 DU) and reducing the standard deviations of tropospheric ozone column differences at high latitudes (by 1 DU for the super Gaussian). Including PAs also makes the retrievals consistent between standard and super Gaussians. This study corroborates the slit function differences between radiance and irradiance, demonstrating that it is important to account for such differences in the ozone profile retrievals.

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The fitting of measured spectra to simulated spectra is the most basic concept for analysis of the Earth's atmospheric constituents from satellite measurements. Therefore, accurate calibration and simulation of measurements are essential for the successful retrieval of atmospheric constituents. The knowledge of the instrumental spectral response function (ISRF) or slit function could affect the accuracies of both calibration and simulation, as it is required for the convolution of a high-resolution reference spectrum to the instrument's spectral resolution in the wavelength calibration and for the convolution of high-resolution absorption cross section spectra or simulated radiance spectra in the calculation of radiance at instrumental resolution. Compared to other trace gases, the retrieval of ozone profiles can be more susceptible to the accuracy of ISRFs due to the large spectral range, where the radiance spans a few orders of magnitude, and to the fact that the spectral fingerprint for the tropospheric ozone is primarily provided by the 310–330 nm absorption features residing in the temperature-dependent Huggins bands. Therefore, the efforts to characterize and verify the ISRFs have preceded the analyses of ozone profiles from satellite and aircraft measurements (X. Liu et al., 2005, 2010; Cai et al., 2012; C. Liu et al., 2015; Sun et al., 2017; Bak et al., 2017).

For spaceborne instruments, ISRFs are typically characterized as a function
of the detector dimensions using a tunable laser source prior to the launch
(Dirksen et al., 2006; Dobber et al., 2009; C. Liu et al., 2015; van Hees et al., 2018) and directly
used in ozone profile retrievals (e.g., Kroon et al., 2011; Mielonen et al.,
2015; Fu et al., 2013, 2018). However, the preflight measured ISRFs could be
inconsistent with those after launch due to the orbital movement and the
instrument temperature change (Beirle et al., 2017; Sun et al., 2017).
Therefore, the post-launch ISRFs have been fitted from the preflight ones
(e.g., Bak et al., 2017; Sun et al., 2017) or parameterized through a
cross correlation of the measured solar irradiance to a high-resolution
solar spectrum (Caspar and Chance, 1997), assuming Gaussian-like shapes
(e.g., X. Liu et al., 2005, 2010). The direct retrieval of the ISRFs from
radiances has not typically been done due to the complication of taking the
atmospheric trace gas absorption and Ring effect into account in the
cross correlation procedure and the slowdown of the fitting process.
However, slit function differences between radiance and irradiance could
exist due to scene heterogeneity, differences in stray light between
radiance and irradiance, and intra-orbit instrumental changes (such as
instrument temperature change) (Beirle et al., 2017; Sun et al., 2017). In
addition, using temporally invariant slit functions derived from
climatological solar spectra in the retrievals could cause long-term
trend errors if instrument degradation occurs. Therefore, there is room for
improving our trace gas retrievals by accounting for the effects of the
different ISRFs between radiance and irradiance on the spectral fitting on a
pixel-to-pixel basis. The pseudo absorber (PA) is a common concept in
spectral fitting to account for the effect of physical phenomena that are
difficult or computationally demanding to simulate in radiative transfer
calculations, like spectral misalignments (shift and stretch) between
radiance and irradiance, Ring effect, spectral undersampling, and additive
stray-light offsets. The pseudo absorption spectrum can be derived from a
finite-difference scheme (e.g., Azam and Richter, 2015) or a linearization
scheme via a Taylor expansion (e.g., Beirle et al., 2013, 2017); the latter
approach is more efficient than the former one, but less accurate because
only the first term of the Taylor series is typically taken into account for
simplicity. Beirle et al. (2013) introduced a linearization scheme to
account for spectral misalignments between radiance and irradiance and then
included them as a pseudo absorber in NO_{2} and BrO fittings based on differential optical absorption spectroscopy (DOAS).
Similarly, Beirle et al. (2017) linearized the effect of the change in the
ISRF parameterized as a super Gaussian on GOME-2 solar irradiance spectra to
characterize the slit function change over time and wavelength. Sun et al. (2017) derived on-orbit slit functions from solar irradiance spectra
measured by the Ozone Monitoring Instrument (OMI) (Levelt et al., 2006)
assuming standard Gaussian, super Gaussian, and preflight ISRFs with
adjusted widths. The derived on-orbit slit functions, showing significant
cross-track dependence that cannot be represented by preflight ISRFs,
substantially improve the retrievals by the Smithsonian Astrophysical
Observatory (SAO) ozone profile algorithm. However, it is not fully
understood why the use of super Gaussian or stretched preflight functions,
which are supposed to better model the OMI spectra as indicated by smaller
mean fitting residuals, does not improve the retrievals over the use of a
standard Gaussian, especially in the standard deviations of the differences relative to ozonesonde observations. This study suggests that the slit
functions derived from solar spectra might not fully represent those in
radiance spectra.

As such, the objective of this paper is to expand the slit function linearization proposed by Beirle et al. (2017) into the optimal-estimation-based spectral fitting of the SAO ozone profile algorithm. The slit function linearization is used to account for the radiative transfer calculation errors caused by the slit functions differences between radiance and irradiance on a pixel-by-pixel basis, and ultimately to improve OMI ozone profile retrievals. This paper is organized as follows: after a mathematical description of the linearization of slit function changes using the generic super Gaussian function, we introduce their practical application in an optimal estimation based spectral fit procedure (Sect. 2). This linearization scheme is implemented differently, depending on the simulation scheme of measured spectra using high resolution or effective cross section data, respectively. Section 3 characterizes the derived pseudo absorber spectra, along with evaluations of ozone profile retrievals using independent ozonesonde observations as a reference dataset. Finally, the summary of this study is given in Sect. 4.

## 2.1 Super Gaussian linearization

The slit function parameterization and linearization are briefly summarized
as in Beirle et al. (2017), focusing on what we need to derive the pseudo
absorbers in the terms of the optimal estimation based fitting process. The
slit function can be parameterized with the slit width *w* and
shape factor *k* assuming the super Gaussian, *S*, to be

where *A*(*w*, *k*) is $\frac{k}{\mathrm{2}{\mathit{\sigma}}_{g}\mathrm{\Gamma}\left(\frac{\mathrm{1}}{w}\right)}$ with Γ representing the gamma function. This
equation allows many forms of distributions by varying *k*: the top-peaked
function (*k**<* 2), the standard Gaussian function (*k*=2), and the
flat-topped function (*k**>* 2). *w* is converted to the full width at
half maximum (FWHM) via the relationship of $\mathrm{FWHM}=\mathrm{2}\sqrt[k]{\mathrm{ln}\mathrm{2}}\phantom{\rule{0.125em}{0ex}}w$ . We investigate the impact of including one more slit parameter *k* on the
OMI ISRF fitting results over the standard Gaussian using OMI daily solar
measurements. As an example, time series (2005–2015) of the fitted slit
width and shape factor in 310–330 nm are displayed in Fig. 1a. The FWHM
and shape factor of the super Gaussian function is on average 0.44 nm and 2.9, respectively, while the FWHM of the standard Gaussian is 0.395 nm. The
sharp change and random-noise of these derived slit function parameters
might be influenced by the decreasing signal-to-noise ratio (SNR) of solar
spectra later in the OMI mission and radiometric errors in solar irradiance
due to the row anomaly (Sun et al., 2017). Figure 1b illustrates the high
wavelength stability (0.003 nm) in the OMI mission, verifying that better
calibration stability is performed with super Gaussian slit functions as
abnormal deviations of wavelength shifts are derived with standard Gaussian
slit functions.

The effect of changing the slit parameters *p* on the slit function can be
linearized by the first-order Taylor expansion approximation
around *S*_{o}=*S*(*p*_{o}):

and thus the effect of changes in *S* on the convolved high-resolution
spectrum can be parameterized as

where the convolved spectrum is $I=S\phantom{\rule{0.125em}{0ex}}\otimes \phantom{\rule{0.125em}{0ex}}{I}_{\mathrm{h}}$. Consequently, the partial derivatives of *I* with respect to slit
parameters *p* are defined as

In Beirle et al. (2017) $\frac{\partial I}{\partial p}$ is referred to as
*J*_{p}, resolution correction spectra (RCS). In Fig. 2, we present an
example of *J*_{p} over the typical ozone profile fitting range (270–330 nm)
through the convolution of high-resolution ozone cross sections (*δ*_{h}) with the derivatives of the super Gaussian $\left(\frac{\partial S}{\partial p}\right)$. The baseline *S*_{o} is defined with
*w*=0.26 nm and *k*=2.6, which are averaged parameters from climatological
OMI solar irradiance spectra in the UV2 band (310–330 nm). Note that this
*w* value corresponds to a FWHM of 0.45 nm. The change in the
assumed OMI slit function causes a highly structured spectral response over
the whole fitting window. However, the relative magnitude of the responses
with respect to both slit parameters is more distinct in the Huggins band
(> 310 nm) where narrow absorption features are observed as shown
in Fig. 2a. An anticorrelation (−0.92) is found between
$\frac{\partial \mathrm{ln}\mathit{\delta}}{\partial w}$ and $\frac{\partial \mathrm{ln}\mathit{\delta}}{\partial k}$ while the response of the unit change of the slit
width to the convolved spectrum is dominant against that of the shape
factor.

## 2.2 Implementation of the slit function linearization in the SAO ozone profile algorithm

In Beirle et al. (2017) a slit function linearization was implemented only
to fit solar irradiances from GOME-2. We implement the slit function
linearization to fit radiances in the SAO ozone profile algorithm (X. Liu et
al., 2010), which is routinely being performed to produce the OMI PROFOZ
product (https://avdc.gsfc.nasa.gov/, last access: 7 July 2019). Two spectral windows (270–309 nm in
the UV1 band and 312–330 nm in the UV2 band) are employed to retrieve ozone
profiles from OMI BUV measurements. To match the different spatial
resolutions between UV1 and UV2 bands, every two cross-track pixels are
averaged for the UV2 band, resulting in 30 positions with the spatial
resolution of 48 km (across-track) × 13 km (along-track) at
nadir position. Partial ozone columns at 24 layers between the surface and
60 km are iteratively estimated toward minimizing the fitting residuals
between measured and simulated radiances and simultaneously between a priori
and estimated ozone values using the optimal estimation inversion method. A
priori ozone information is taken from a tropopause-based (TB) ozone profile
climatology (Bak et al., 2013). The vector linearized discrete ordinate
radiative transfer model (VLIDORT; Spurr, 2008) is used to simulate the
radiances and their derivatives with respect to geophysical parameters. The
radiance calculation is made for the Rayleigh atmosphere, where the incoming
sunlight is simply absorbed by ozone and other trace gases, scattered by air
molecules, and reflected by surfaces/clouds assumed as a Lambertian surface.
In addition to these, other physical phenomena are treated as PAs to the spectral
response such as Ring effect, additive offset, and spectral shifts due to
misalignments of radiance relative to irradiance and ozone cross sections.
In the SAO algorithm, these PAs are derived using finite differences of the
radiances with and without perturbation to a phenomenon, except for the Ring
spectrum that is calculated using a first-order single-scattering rotational
Raman scattering model (Sioris and Evans, 2000). In this paper, we introduce
new PAs to account for the radiance simulation errors caused by the slit
function errors. The OMI ISRFs have been parameterized as a standard
Gaussian from climatological OMI solar irradiances for each UV1 and UV2 band
and thereby these PAs could take into account the spectral fitting responses
caused by temporal variations in the slit function. This ozone fitting
procedure uses ISRFs to convolve high-resolution absorption spectra, taken
from Brion et al. (1993) for ozone absorption cross sections and Wilmouth et
al. (1999) for BrO absorption cross sections. In DOAS analysis, the pseudo
absorber is defined as $\frac{\partial S}{\partial p}\phantom{\rule{0.125em}{0ex}}\otimes \phantom{\rule{0.125em}{0ex}}{\mathit{\sigma}}_{\mathrm{h}}$ (*σ*_{h} is a
high-resolution absorption cross section), which could be calculated at a
computationally low cost. In our optimal-estimation-based ozone profile
retrievals, it is conceptually defined as $\frac{\partial S}{\partial p}\phantom{\rule{0.125em}{0ex}}\otimes \phantom{\rule{0.125em}{0ex}}{I}_{\mathrm{h}}$ (*I*_{h} is a
high-resolution simulated radiance), which is computationally very expensive
because of online radiative calculation for a ∼60 nm wide
fit window on the spatial pixel-to-pixel basis. We now introduce how to
implement the slit function linearization to derive the derivatives of the
OMI radiances with respect to slit function changes in two different
radiative transfer approaches used in the SAO ozone profile algorithm, i.e.,
the effective cross section approach in X. Liu et al. (2010) and the updated
high-resolution convolution approach described in Kim et al. (2013).

In X. Liu et al. (2010), VLIDORT simulates the radiances at OMI spectral grids
(*λ*_{omi}) using effective cross sections that are
produced by convolving high-resolution cross sections with the OMI ISRFs.
Therefore, we apply a similar convolution process of matching the
high-resolution cross section spectra with OMI spectra to derive the partial
derivative of *σ*_{x} with respect to slit parameter *p* as follows:

where *σ*_{x,h} is a high-resolution absorption spectrum for ozone
or BrO. Due to the dominant absorption of O_{3} over BrO, the derivative
of the BrO cross section with respect to *p* is neglected here. This partial
derivative of ozone is then converted to the partial derivative of radiance
through the chain rule with the analytical ozone weighting function
($\frac{\mathrm{dln}I}{{\mathrm{dO}}_{\mathrm{3}}}$), calculated from
VLIDORT, as follows:

This simulation process is hereafter referred to as effective resolution cross section (ER) simulation.

As described in Kim et al. (2013), the radiative transfer calculation in the SAO ozone profile algorithm has been performed using high-resolution extinction spectra at the optimized sampling intervals for resolving the ozone absorption features, which are ∼1.0 nm below 300 nm and ∼0.4 nm above 300 nm. These sampling intervals are coarser than actual OMI sampling grids with approximately half the number of wavelengths. The coarser sampled simulated radiances are then interpolated to a fine grid of 0.05 nm assisted by the weighting functions with respect to absorption and Rayleigh optical depth:

where ${\mathrm{\Delta}}_{\mathrm{l}}^{\mathrm{gas}}$ and ${\mathrm{\Delta}}_{\mathrm{l}}^{\mathrm{ray}}$ are
the optical thickness (the product of cross section and layer column
density) at each layer for trace gas absorption and Rayleigh scattering,
respectively. The convolution is then applied to these simulated
high-resolution radiances *I*(*λ*_{h}) with
assumed slit functions and derivatives and thereby
*I*(*λ*_{omi}) and $\frac{\partial \mathrm{ln}I}{\partial p}$ are calculated. This
simulation process is hereafter referred to as high-resolution cross
section (HR) simulation. The ER simulation is more commonly implemented in
trace gas retrievals in the UV and visible ranges, but the HR simulation allows for
more accurate fitting residuals, to better than 0.1 % (Kim et al., 2013)
as well as shorter computation time. $\frac{\partial \mathrm{ln}I}{\partial p}$ is scaled by the fitting coefficients,
Δ*p* to account for the actual size of the spectral
structures caused by the slit function differences between radiance and
irradiance spectra. The pseudo absorber (PA) for the super Gaussian slit
function linearization is expressed as

In the form of the logarithm of normalized radiance, PA is physically
related to the optical depth change Δ*τ*. Figure 3
compares the partial derivatives of radiances to slit parameters
$\frac{\mathrm{dln}I}{\mathrm{d}p}$ in HR and ER simulations. Little difference is found even
though convolution error for ozone cross sections is only accounted for in
the ER simulation due to the overwhelming impact of ozone cross section
convolution errors over other cross section data. The amplitude of
$\frac{\mathrm{dln}I}{\mathrm{d}p}$ varies with different satellite pixels (e.g., ozone
profile shape, geometry, and cloud/surface property), but the spectral peak
positions do not change because they arise from the errors due to the
convolution process of high-resolution absorption cross sections dominated
by ozone. It should be noted that these spectral structures are weakly
correlated with the partial derivatives of radiances with respect to other
state vectors (ozone, BrO, cloud fraction, surface albedo,
radiance–irradiance shift, radiance–ozone cross section shift, Ring, mean
fitting residual scaling factor) within ±0.3 and ±0.1 in the UV1 and UV2, respectively.

Furthermore, this linearization process can be formulated with *n*-order
polynomial fitting parameters (Δ*p*_{i}) to
account for the wavelength-dependent change in the slit parameters around a
central wavelength $\stackrel{\mathrm{\u203e}}{\mathit{\lambda}}$ , which is expressed as

We characterize the effect of including the PA $(\frac{\partial \mathrm{ln}I}{\partial p}\cdot p)$ on ozone profile
retrievals using both super Gaussian and standard Gaussian slit functions.
Hereafter, the correction spectrum $\left(\frac{\partial \mathrm{ln}I}{\partial p}\right)$ is derived using the HR simulation.
The PA coefficient (Δ*p*_{i}) (one for each channel
and for each order) is included as part of the state vector to be
iteratively and simultaneously retrieved with ozone. The a priori value is
set to be zero for all fitting coefficients, while the a priori error is set
to be 0.1, empirically. We should note that the empirical “soft
calibration” is applied to OMI radiances before the spectral fitting, in
order to eliminate the wavelength- and cross-track-dependent systematic
biases, due to the interference of the PA coefficients with systematic
measurement errors during the fitting process.

## 3.1 Characterization of the pseudo absorbers in ozone fitting procedure

Figure 4 displays how the zero-order PA coefficients (Δ*p*) vary
within one orbit when slit functions are assumed to be standard and super
Gaussians along with variation in cloud fraction, surface
albedo, and cloud pressure from the retrievals. These retrieved coefficients
physically represent the deviation of ISRFs in radiances from those in solar
measurements. We normalize them with the slit parameters derived from OMI
solar irradiances for a better interpretation. Cross-track-dependent
features are shown in slit width. The relative change in the slit width is
more distinct in the UV1 band than in the UV2 band, whereas the change in
the shape factor is more distinct in the UV2 band. The UV2 slit widths
increase typically within 5 % over the given spatial domain. However, the
UV1 slit widths increase from 10 % at most pixels up to 50 % at
off-nadir positions in the high latitudes, which might be caused by stray
light differences between radiance and irradiance and intra-orbit
instrumental changes. An abnormal change in the UV1 slit parameters due to
the scene heterogeneity is detected at the along-track scan positions of
∼300 and 900 where upper-level clouds are
present. The UV2 shape factor changes show a coherent sensitivity to bright
surfaces under clear-sky conditions over the northern high latitudes. Fitting
coefficients for the standard Gaussian show a quite similar spatial
variation for the UV1 slit width (correlation = ∼0.98), but
an anticorrelation of $\sim -\mathrm{0.62}$ for the UV2 slit width compared
to that for a super Gaussian due to the interference between shape factor and
slit width.

Examples of the PAs (Eq. 9) are illustrated in Fig. 5 when (a) zero- and (b) first-order polynomial coefficients are fitted. In the UV1 range, the sum of PAs multiplied by corresponding coefficients, regardless of which Gaussian is assumed as the slit function, is very similar because the spectral structure caused by the slit width change is dominant. It implies that OMI ISRFs in the UV1 band are similar to the standard Gaussian, for both radiance and irradiance measurements, consistent with the pre-launch characterization (Dirksen et al., 2006). However, in the UV2 range, the spectral structures are generated by the shape factor change rather than the slit width change and therefore PAs show noticeable discrepancies for different Gaussian assumptions. Our results indicate that the PA for the shape factor change is required to adjust the spectral structures due to the differences in the slit functions between radiance and irradiance over the UV2 band. In the case of the wavelength-dependent PA coefficient fit, the impact of first-order PAs on OMI radiances is relatively visible in the wavelength range of 300–310 nm. This result is physically consistent with the wavelength-dependent property shown in the slit parameters derived from OMI irradiances as shown in Fig. 6 where slit parameters are characterized in 10-pixel increments assuming the super Gaussian slit function. In UV1, the slit widths plotted as FWHM slightly decrease by ∼0.1 nm at shorter wavelengths than 288 nm, but vary more sharply by up to ∼0.2 nm at longer wavelengths. Compared to slit widths, the wavelength dependences of the shape factors are less noticeable, except at boundaries of the window. In the UV2 window, both slit width and shape factor are highly invariant.

## 3.2 Impact of including pseudo absorbers on ozone profile retrievals

Figures 7 to 9 evaluate the impact of including zero-order PAs on ozone profile retrievals. Figure 7 illustrates how different assumptions in the slit functions affect the ozone profile retrievals with respect to the retrieval sensitivity and the fitting accuracy from the case shown in Fig. 4. In this figure, the degrees of freedom for signal (DFS) represent the independent pieces of ozone information available from measurements, which typically decreases as ozone retrievals are further constrained by other fitting variables. The reduced DFS values (< 5 %) imply that the ozone retrievals are correlated slightly with PAs. The fitting accuracy is assessed as the root mean square (rms) of the relative differences ( %) between measured and calculated radiances over the UV1 and UV2 ranges. Including the PAs makes little difference in the UV1 fitting residuals for most of individual pixels (1 %–5 %), but significantly reduces residuals in the UV2 range. The adjusted amounts of the residuals with PAs are generally larger when assuming super Gaussian slit functions. This comes from different assumptions for slit functions in deriving soft calibration spectra, where slit functions were parameterized as standard Gaussians. Therefore, applying soft calibration to OMI spectra entails somewhat artificial spectral structures if ISRFs are assumed as super Gaussian in ozone retrievals, and hence the impact of PAs on the spectral fitting becomes more considerable. Figure 8 compares how the spectral residuals are adjusted with PAs when soft calibration is turned on and off. Using super Gaussians causes larger amplitudes of the spectral fitting residuals than using standard Gaussians, if soft calibration is turned on and PAs are excluded. Conversely, some residuals are reduced and more broadly structured if soft calibration is turned off. Including PAs eliminates or reduces some spikes of fitting residuals as well as improves the consistency of the fitting accuracy between using standard and super Gaussians at wavelengths above 300 nm.

The benefit of this implementation for ozone retrievals is further assessed
through comparison with electrochemical concentration cell (ECC) ozonesondes
collected from the WOUDC (https://woudc.org/, last access: 7 July 2019) and SHADOZ
(https://tropo.gsfc.nasa.gov/shadoz/, last access: 7 July 2019) networks. This evaluation is limited
to the period of 2005 through 2008 to avoid interferences with row-anomaly
effects appearing in 2007 and becoming serious in early 2009 (Schenkeveld
et al., 2017). We select 13 SHADOZ sites in the tropics and 38 WOUDC sites in
the northern midlatitudes to high latitudes. The collocation criteria are within ±1^{∘} in latitude and longitude and within 12 h in time. For
comparison, high-vertical-resolution (∼100 nm) profiles of
ozonesondes are interpolated onto OMI retrieval grids (∼2.5 km thick). We limit OMI–ozonesonde comparisons to OMI solar zenith angle
< 85^{∘}, effective cloud fraction < 0.4, surface
albedo < 20 % (100 %) in the tropics and midlatitudes (high
latitude), top altitude of ozonesondes > 30 km, ozonesonde
correction factors ranging from 0.85 to 1.15 if they exist, and data gaps
for each ozonesonde no greater than 3 km. Comparisons between OMI and
ozonesondes are performed for the tropospheric ozone columns (TCOs) over three
different latitude bands and for ozone profiles including all the sites,
with and without PAs (zero order) for standard and super Gaussian slit
function changes.

In Table 1, the comparison statistics of tropospheric ozone columns between
OMI and ozonesonde are summarized as a function of latitude bands. Without
using PAs, the comparison results show a noticeable discrepancy in mean
biases (1.3–2.1 DU or 3.9 %–6.4 %) due to different assumptions on the slit
function shape, with positive biases of 0.3–0.7 DU for super Gaussians and
negative biases of 1.0–1.4 DU for standard Gaussians. Overall, OMI
retrievals are in a better agreement with ozonesonde measurements using
super Gaussians. The correlations and standard deviations are very similar
in the tropics and midlatitudes, but the retrievals with standard Gaussians
show better correlation and smaller standard deviations at high latitudes.
As in Sun et al. (2017), the retrievals show significant differences between
using standard and super Gaussians, although there are some inconsistencies
in comparing OMI and ozonesondes; the main inconsistent factors are as follows. In this
study, soft calibration is turned on and a priori information is taken from
the TB climatology to perform OMI ozone profile retrievals, whereas soft
calibration is turned off and a priori information is taken from the Labow–Logan McPeters (LLM)
climatology (McPeters et al., 2007) in Sun et al. (2017). OMI and ozonesonde data filtering criteria are
quite similar to each other, except that the criteria of the solar zenith
angle and cloud fraction are relaxed from 75^{∘} and 0.3 to
85^{∘} and 0.4, respectively, and the adjustment of ozonesondes with
correction factors given for the WOUDC dataset is turned on in this study.
Comparison is performed by latitudes here whereas global comparison is
analyzed in Sun et al. (2017). After accounting for the slit differences
between radiances and irradiances using PAs, the retrievals are improved for
both standard and super Gaussians and these two retrievals become consistent
except for the use of super Gaussians in the tropics. The mean biases in the
tropics and midlatitudes are almost eliminated, but the standard deviations
and correlation do not change much. In the high latitudes, the standard
deviations and correlation are significantly improved due to applying PAs
with super Gaussian ISRFs. The lack of improvement with PAs in the tropics
with super Gaussians illustrates that ISRFs of radiances are quite similar
to those of irradiances in the tropics, while super Gaussians better
parameterize OMI ISRFs than standard Gaussians. This is consistent with the
comparison of the fitting accuracy of the UV2 band as shown in Fig. 7,
where the fitting residuals are slightly reduced in the tropics when super
Gaussians are linearized, but the standard Gaussian linearization
significantly improves the fitting accuracy. The mean biases of the profile
comparison as shown in Fig. 9 clearly show that including PAs to account
for ISRF differences reduces mean biases by up to ∼5 %
below 10 km and their general altitude dependence and improves the
consistency between using standard and super Gaussians; in addition, the
standard deviations are slightly improved in the 10–20 km altitude range for
both Gaussians. The improvement at all latitudes corroborates the change in
ISRFs between radiance and irradiance along the orbit as conjectured by Sun
et al. (2017). The consistency between using standard and super Gaussians
after using PAs is mainly because there is strong anticorrelation between
the slit width and shape partial derivatives as shown in Fig. 2, so the
adjustment of slit width only in the use of standard Gaussians can achieve
almost the same effect as the adjustment of both parameters in the use of
super Gaussians. Accounting for the wavelength-dependent change in the ISRFs
with first-order PAs makes insignificant differences to both fit residuals
and ozone retrievals (not shown here). This could be mainly explained by negligible wavelength dependence of OMI ISRFs especially in UV2 as
shown in Fig. 5, where the PA spectrum ($\frac{\partial \mathrm{ln}I}{\partial p}\cdot \mathrm{\Delta}p$) shows almost no variance except at the upper
boundary of UV1, as well as in Fig. 6 where the UV2 slit parameters
derived from irradiances in the sub-fit windows vary within 0.05 nm for FWHM
and 0.2 for shape factor.

Knowledge of the instrument spectral response functions (ISRFs) or slit functions is important for ozone profile retrievals from the Hartley and Huggins bands. ISRFs can be measured in the laboratory prior to launch, but they have been typically derived from solar irradiance measurements assuming Gaussian-like functions in order to account for the effect of the ISRF changes after launch. However, the parameterization of the ISRFs from solar irradiances could be inadequate for achieving a high accuracy of the fitting residuals as ISRFs in radiances could significantly deviate from those in solar radiances (Beirle et al., 2017) and might affect ozone profile retrievals as suggested in Sun et al. (2017). Therefore, this study implements a linearization scheme to account for the spectral errors caused by the ISRF changes as pseudo absorbers (PAs) in an optimal-estimation-based fitting procedure for retrieving ozone profiles from OMI BUV measurements using the SAO ozone profile algorithm. The ISRFs are assumed to be the generic super Gaussian that can be used as standard Gaussians when fixing the shape factor to 2. This linearization was originally introduced in Beirle et al. (2017) for DOAS analysis, but this study extends this application and provides more details on how to implement in practice using two different approaches to derive radiance errors from slit function partial derivatives with respect to slit parameters. These two approaches correspond to the two methods of simulating radiances at instrument spectral resolution, one using effective cross sections, which were previously used in the SAO ozone profile algorithm and are still used in most of the trace gas retrievals from the UV and visible, and the other calculating radiances at high resolution before convolution, which is the preferred method in the SAO ozone profile algorithm. Consistent PAs are derived with these two approaches, as expected.

The fitting coefficients (Δ*p*) to the PAs, representing the
difference of slit parameters between radiance and irradiance, are
iteratively fitted as part of the state vector along with ozone and other
parameters. The UV1 slit parameters show distinct cross-track-dependent
differences, especially in high latitudes. In addition, an abnormal
Δ*p* caused by scene heterogeneity is observed around bright
surfaces and cloudy scenes. The PA spectrum $(\frac{\partial I}{\partial p}\cdot \mathrm{\Delta}p)$ illustrates that the slit
width change causes most of the spectral structures in the UV1 band because
the OMI ISRFs are close to Gaussian. Otherwise, the ISRF change results in
different spectral responses in the UV2 band with different Gaussian
functions because the adjustment of the shape factor becomes more important
in accounting for the convolution error when using super Gaussians.

Insignificant wavelength dependence on OMI slit functions is demonstrated from slit function parameters derived from irradiances in the sub-fit window, which leads to little difference in ozone profile retrievals when zero- and first-order wavelength-dependent PA coefficients are implemented to fit the spectral structures caused by slit function errors. Therefore we evaluate the benefit of including the zero-order PA fit for both the accuracy of the fitting residuals and the quality of retrieved ozone profiles through validation against ozonesonde observations. Some spikes in the fitting residuals are reduced or eliminated. Commonly, including PAs makes little change in both fit residuals and ozone retrievals in the tropics if super Gaussians are assumed as ISRFs but this is not the case for the standard Gaussian assumption. In the TCO comparison between OMI and ozonesonde, the mean biases are reduced by 0.2 (0.6) and 0.6 (1.4) DU in the tropics (midlatitude) when super and standard Gaussians are linearized, respectively. In particular, applying PA improves the standard deviations at high latitudes by 1.0 DU for super Gaussians and 0.5 DU for standard Gaussians. The profile comparison generally shows improvements in mean biases (∼5 % in the lower troposphere) as well as in standard deviation, slightly in the altitude range 10–20 km by applying PAs. More importantly, using these PAs makes the retrieval consistent between standard and super Gaussians. Such consistency is due to the anticorrelation between slit width and shape PAs. This study demonstrates the slit function differences between radiance and irradiance and their usefulness to account for such differences on a pixel-to-pixel basis. In this experiment, the soft spectrum, derived with the standard Gaussian assumption, is applied to remove systematic measurement errors before spectral fitting, indicating that the evaluation of ozone retrievals might be unfairly performed for the super Gaussian function implementation. Nonetheless, OMI ozone profile retrievals show better agreement with ozonesonde observations when the super Gaussian is linearized. Actually, the fitting residuals are slightly more broadly structured with super Gaussians than with standard Gaussians if the soft calibration and PAs are turned off, indicating the benefit of deriving a soft calibration with the super Gaussians. Therefore, there is still room for achieving better benefits when using the PAs on ozone profile retrievals by applying the soft calibration derived with super Gaussians.

The OMI Level 1 B radiance product are available at https://aura.gesdisc.eosdis.nasa.gov/data/Aura_OMI_Level1/OML1BRUG.003/ (last access: 7 July 2019, Dobber, 2007). The WOUDC ozonesonde dataset are https://woudc.org/data/products/ozonesonde/ (last access: 7 July 2019, WMO-GAW, 2019) and SHADOZ ozonesonde dataset are available at https://tropo.gsfc.nasa.gov/shadoz/Archive.html (last access: 7 July 2019, Thompson et al., 2017; Witte et al., 2017).

JB and XL designed the research; XL provided oversight and guidance; KS and JB developed the methodology together; JB conducted the research and wrote the paper; XL, SK, KC, and JHK contributed to the analysis and writing.

The authors declare that they have no conflict of interest.

We acknowledge the OMI science team for providing their satellite data and the WOUDC and SHADOZ networks for their ozonesonde datasets. Research at the Smithsonian Astrophysical Observatory by Juseon Bak, Xiong Liu, Kang Sun, and Kelly Chance was funded by NASA Aura science team program (NNX14AF16G, NNX17AI82G). Research at Pusan National University by Jae-Hwan Kim was supported by the Korea Ministry of Environment (MOE) in the form of the Public Technology Program based on environmental policy (2017000160001).

This research has been supported by NASA Aura science team program (grant nos. NNX14AF16G, NNX17AI82G).

This paper was edited by John Worden and reviewed by two anonymous referees.

Azam, F. and Richter, A.: GOME2 on MetOp: Follow on analysis of GOME2 in orbit degradation, Final report, EUM/CO/09/4600000696/RM, available at: https://www.eumetsat.int/website/wcm/idc/idcplg?IdcService=GET_FILE&dDocName=PDF_GOME_DEG_REP&RevisionSelectionMethod=LatestReleased&Rendition=Web (last access: 7 September 2016), 2015.

Bak, J., Liu, X., Wei, J. C., Pan, L. L., Chance, K., and Kim, J. H.: Improvement of OMI ozone profile retrievals in the upper troposphere and lower stratosphere by the use of a tropopause-based ozone profile climatology, Atmos. Meas. Tech., 6, 2239–2254, https://doi.org/10.5194/amt-6-2239-2013, 2013.

Bak, J., Liu, X., Kim, J.-H., Haffner, D. P., Chance, K., Yang, K., and Sun, K.: Characterization and correction of OMPS nadir mapper measurements for ozone profile retrievals, Atmos. Meas. Tech., 10, 4373–4388, https://doi.org/10.5194/amt-10-4373-2017, 2017.

Beirle, S., Sihler, H., and Wagner, T.: Linearisation of the effects of spectral shift and stretch in DOAS analysis, Atmos. Meas. Tech., 6, 661–675, https://doi.org/10.5194/amt-6-661-2013, 2013.

Beirle, S., Lampel, J., Lerot, C., Sihler, H., and Wagner, T.: Parameterizing the instrumental spectral response function and its changes by a super-Gaussian and its derivatives, Atmos. Meas. Tech., 10, 581–598, https://doi.org/10.5194/amt-10-581-2017, 2017.

Brion, J., Chakir, A., Daumont, D., and Malicet, J.: High-resolution
laboratory absorption cross section of O_{3}, Temperature effect, Chem. Phys.
Lett., 213, 610–612, 1993.

Cai, Z., Liu, Y., Liu, X., Chance, K., Nowlan, C. R., Lang, R., Munro, R., and Suleiman, R.: Characterization and correction of Global Ozone Monitoring Experiment 2 ultraviolet measurements and application to ozone profile retrievals, J. Geophys. Res., 117, D07305, https://doi.org/10.1029/2011JD017096, 2012.

Caspar, C. and Chance, K.: GOME wavelength calibration using solar and atmospheric spectra, Third ERS Symposium on Space at the Service of our Environment, Florence, Italy, 14–21 March, 1997.

Dirksen, R., Dobber, M., Voors, R., and Levelt, P.: Prelaunch characterization of the Ozone Monitoring Instrument transfer function in the spectral domain, Appl. Opt., 45, 3972–3981, https://doi.org/10.1364/AO.45.003972, 2006.

Dobber, M.: OMI/Aura Level 1B UV Global Geolocated Earthshine Radiances 1-orbit L2 Swath 13m × 24 km V003, Greenbelt, MD, USA, Goddard Earth Sciences Data and Information Services Center (GES DISC), https://doi.org/10.5067/Aura/OMI/DATA1002 (last access: 7 July 2019), 2007.

Dobber, M., Voors, R., Dirksen, R., Kleipool, Q., and Levelt, P.: The high-resolution solar reference spectrum between 250 and 550 nm and its application to measurements with the Ozone Monitoring Instrument, Sol. Phys., 249, 281–291, 2008.

Fu, D., Worden, J. R., Liu, X., Kulawik, S. S., Bowman, K. W., and Natraj, V.: Characterization of ozone profiles derived from Aura TES and OMI radiances, Atmos. Chem. Phys., 13, 3445–3462, https://doi.org/10.5194/acp-13-3445-2013, 2013.

Fu, D., Kulawik, S. S., Miyazaki, K., Bowman, K. W., Worden, J. R., Eldering, A., Livesey, N. J., Teixeira, J., Irion, F. W., Herman, R. L., Osterman, G. B., Liu, X., Levelt, P. F., Thompson, A. M., and Luo, M.: Retrievals of tropospheric ozone profiles from the synergism of AIRS and OMI: methodology and validation, Atmos. Meas. Tech., 11, 5587–5605, https://doi.org/10.5194/amt-11-5587-2018, 2018.

Kim, P. S., Jacob, D. J., Liu, X., Warner, J. X., Yang, K., Chance, K., Thouret, V., and Nedelec, P.: Global ozone–CO correlations from OMI and AIRS: constraints on tropospheric ozone sources, Atmos. Chem. Phys., 13, 9321–9335, https://doi.org/10.5194/acp-13-9321-2013, 2013.

Kroon, M., de Haan, J. F., Veefkind, J. P., Froidevaux, L., Wang,R., Kivi, R., and Hakkarainen, J. J.: Validation of operational ozone profiles from the Ozone Monitoring Instrument, J. Geophys. Res., 116, D18305, https://doi.org/10.1029/2010JD015100, 2011.

Levelt, P. F., van den Oord, G. H. J., Dobber, M. R., Malkki, A., Visser, H., de Vries, J., Stammes, P., Lundell, J. O. V., and Saari, H.: The ozone monitoring instrument, IEEE Trans. Geosci. Remote Sens., 44, 1093–1101, https://doi.org/10.1109/TGRS.2006.872333, 2006.

Liu, C., Liu, X., Kowalewski, M. G., Janz, S. J., González Abad, G., Pickering, K. E., Chance, K., and Lamsal., L. N.: Characterization and verification of ACAM slit functions for trace gas retrievals during the 2011 DISCOVER-AQ flight campaign, Atmos. Meas. Tech., 8, 751–759, https://doi.org/10.5194/amt-8-751-2015, 2015.

Liu, X., Chance, K., Sioris, C. E., Spurr, R. J. D., Kurosu, T. P., Martin, R. V., and Newchurch, M. J.: Ozone profile and tropospheric ozone retrievals from Global Ozone Monitoring Experiment: algorithm description and validation, J. Geophys. Res., 110, D20307, https://doi.org/10.1029/2005JD006240, 2005.

Liu, X., Bhartia, P. K., Chance, K., Spurr, R. J. D., and Kurosu, T. P.: Ozone profile retrievals from the Ozone Monitoring Instrument, Atmos. Chem. Phys., 10, 2521–2537, https://doi.org/10.5194/acp-10-2521-2010, 2010.

McPeters, R. D., Labow, G. J., and Logan, J. A.: Ozone climatological profiles for satellite retrieval algorithms, J. Geophys. Res., 112, D05308, https://doi.org/10.1029/2005JD006823"10.1029/2005JD006823, 2007.

Mielonen, T., de Haan, J. F., van Peet, J. C. A., Eremenko, M., and Veefkind, J. P.: Towards the retrieval of tropospheric ozone with the Ozone Monitoring Instrument (OMI), Atmos. Meas. Tech., 8, 671–687, https://doi.org/10.5194/amt-8-671-2015, 2015.

Schenkeveld, V. M. E., Jaross, G., Marchenko, S., Haffner, D., Kleipool, Q. L., Rozemeijer, N. C., Veefkind, J. P., and Levelt, P. F.: In-flight performance of the Ozone Monitoring Instrument, Atmos. Meas. Tech., 10, 1957–1986, https://doi.org/10.5194/amt-10-1957-2017, 2017.

Sioris, C. E. and Evans, W. F. J.: Impact of rotational Raman scattering in
the O_{2} A band, Geophys. Res. Lett., 27, 4085–4088, 2000.

Spurr, R. J. D.: Linearized pseudo-spherical scalar and vector discrete ordinate radiative transfer models for use in remote sensing retrieval problems, in: Light Scattering Reviews, edited by: Kokhanovsky, A., Springer, New York, 229–275, 2008.

Sun, K., Liu, X., Huang, G., González Abad, G., Cai, Z., Chance, K., and Yang, K.: Deriving the slit functions from OMI solar observations and its implications for ozone-profile retrieval, Atmos. Meas. Tech., 10, 3677–3695, https://doi.org/10.5194/amt-10-3677-2017, 2017.

Thompson, A. M., Witte, J. C., Sterling, C., Jordan, A., Johnson, B. J., Oltmans, S. J., Fujiwara, M. Vömel, H. Allaart, M., Piters, A., Coetzee, J. G. R., Posny, F., Corrales, E., Andres Diaz, J., Félix, C., Komala, N., Lai, N. Maata, M., Mani, F., Zainal, Z., Ogino, S-Y., Paredes, F., Bezerra Penha, T. L., Raimundo da Silva, F., Sallons-Mitro, S., Selkirk, H. B., Schmidlin, F. J., Stuebi, R., and Thiongo, K.: First reprocessing of Southern Hemisphere Additional Ozonesondes (SHADOZ) Ozone Profiles (1998–2016), 2. Comparisons with satellites and ground-based instruments, J. Geophys. Res., JD027406, https://doi.org/10.1002/2017JD027406, 2017.

van Hees, R. M., Tol, P. J. J., Cadot, S., Krijger, M., Persijn, S. T., van Kempen, T. A., Snel, R., Aben, I., and Hoogeveen, Ruud W. M.: Determination of the TROPOMI-SWIR instrument spectral response function, Atmos. Meas. Tech., 11, 3917–3933, https://doi.org/10.5194/amt-11-3917-2018, 2018.

Wilmouth, D. M., Hanisco, T. F., Donahue, N. M., and Anderson, J. G.: Fourier transform ultraviolet spectroscopy of the ${A}^{\mathrm{2}}I{I}_{\mathrm{3}/\mathrm{2}}-{X}^{\mathrm{2}}I{I}_{\mathrm{3}/\mathrm{2}}$ Transition of BrO, J. Phys. Chem. A., 103, 8935–8945, 1999.

Witte, J. C., Thompson, A. M., Smit, H. G. J., Fujiwara, M., Posny, F., Coetzee, G. J. R., Northam, E. T., Johnson, B. J., Sterling, C. W., Mohamad, M., Ogino, S.-Y., Jordan, A., and da Silva, F. R.: First reprocessing of Southern Hemisphere Additional OZonesondes (SHADOZ) profile records (1998–2015): 1. Methodology and evaluation, J. Geophys. Res. Atmos., 122, 6611–6636, 2017.

World Meteorological Organization-Global Atmosphere Watch Program (WMO-GAW)/World Ozone and Ultraviolet Radiation Data Centre (WOUDC) ozonesonde dataWMO/GAW Ozone Monitoring Community https://doi.org/10.14287/10000008, 2019.