Diurnal carbon monoxide observed from a geostationary infrared hyperspectral sounder: first result from GIIRS on board FengYun-4B

Abstract

The Geostationary Interferometric Infrared Sounder (GIIRS) on board FengYun-4 series satellites is the world's first geostationary hyperspectral infrared sounder. With hyperspectral measurement collected from a geostationary orbit covering the carbon monoxide (CO) absorption window around 2150 cm${}^{-\mathrm{1}}$, GIIRS provides a unique opportunity for monitoring the diurnal variabilities of atmospheric CO over eastern Asia. In this study, we develop the FengYun Geostationary satellite Atmospheric Infrared Retrieval (FY-GeoAIR) algorithm to retrieve the CO profiles using observations from GIIRS on board FY-4B, which was launched in June 2021, and provide CO maps at a spatial resolution of 12 km and a temporal resolution of 2 h. The performance of the algorithm is first evaluated by conducting retrieval experiments using simulated synthetic spectra. The result shows that the GIIRS data provide significant information for constraining CO profiles. The degree of freedom for signal (DOFS) and retrieval error are both highly correlated with thermal contrast (TC), the temperature difference between the surface and the lower atmosphere. Retrieval results from 1 month of GIIRS spectra in July 2022 show that the DOFS for the majority is between 0.8 and 1.5 for the CO total column and between 0 and 0.8 for the bottom three layers ranging from the surface to 3 km a.s.l. Consistent with CO retrievals from low-Earth-orbit (LEO) infrared sounders, the largest observation sensitivity, as quantified by the averaging kernel (AK), is in the free troposphere at around 3–6 km. The diurnal changes in DOFS and vertical sensitivity of observation are primarily driven by the diurnal TC variabilities. Finally, we compare the CO total columns between GIIRS and Infrared Atmospheric Sounding Interferometer (IASI) and find that the two datasets show good consistency in capturing the spatial and temporal variabilities. This study demonstrates that the GIIRS retrievals are able to reproduce the temporal variability of CO total columns over eastern Asia in the daytime in July. Nevertheless, the retrievals have low detectivity in the nighttime due to their weak sensitivity to the ground level CO changes limited by low information content. Model assimilation that takes into account the retrieved diurnal CO profiles and the associated vertical sensitivity will have potential in improving local and global air quality and climate research over eastern Asia.

1 Introduction

Observing atmospheric composition from space provides critical data for forecasting air quality, assessing climate change and monitoring the long-term variabilities in tropospheric and stratospheric compositions. In the last two decades, satellite-borne instruments on board polar-orbiting satellites in low-Earth orbit (LEO) have demonstrated their full capabilities in observing the atmospheric composition (e.g., Clerbaux et al., 2003; Crevoisier et al., 2014; Shephard et al., 2015; Buchwitz et al., 2005; Borsdorff et al., 2018). However, a single LEO satellite has a revisit time of 12 h over the Equator. In general, only one (for near-infrared or UV–visible instrument) or two (for thermal infrared sounder) observations are available each day for the same spot. Critical information on the diurnal cycle of atmospheric composition is, however, not available from LEO satellites. As an important advancement over current LEO instruments, measurements from geostationary (GEO) orbit can provide contiguous coverage with similar or higher spatial resolution and a revisit time of 1–2 h, which would provide breakthrough measurements for numerical weather prediction and support high-temporal-resolution air quality forecasting (Schmit et al., 2009).

The Geostationary Interferometric Infrared Sounder (GIIRS) on board FengYun-4 series satellites, launched in 2016 (FY-4A) and 2021 (FY-4B), respectively, is the world's first geostationary hyperspectral infrared sounder (Yang et al., 2017). With a spectral resolution of 0.625 cm${}^{-\mathrm{1}}$, similar to current LEO satellites, GIIRS provides a unique opportunity for observing the diurnal variabilities of atmospheric composition over eastern Asia, as has been demonstrated in retrieving atmospheric ammonia (Clarisse et al., 2021). Existing on-orbit GEO instruments for observing air quality also include the Geostationary Environment Monitoring Spectrometer (GEMS) by South Korea, which was launched in February 2020. GEMS was designed to measure air quality in Asia using ultraviolet and visible (UV–VIS) bands (Kim et al., 2020). Future GEO missions with hyperspectral capabilities include ESA's Sentinel-4 mission on board the Meteosat Third Generation Sounder platform, which is made up of the thermal Infrared Sounder (IRS) for providing profiles of temperature and humidity and the ultraviolet–visible–near-infrared (UVN) spectrometer for monitoring air quality trace gases and aerosols in Europe (Ingmann et al., 2012; Holmlund et al., 2021), and NASA's Tropospheric Emissions: Monitoring of Pollution (TEMPO; Zoogman et al., 2017) that will track air quality in North America. In addition, the to-be-launched greenhouse gas targeted mission Geostationary Carbon Cycle Observatory (GeoCarb) by NASA was designed to measure carbon dioxide (CO${}_{\mathrm{2}}$), methane (CH${}_{\mathrm{4}}$) and carbon monoxide (CO) throughout the Americas (Polonsky et al., 2014).

As an important trace gas for understanding air quality and climate forcing, CO is a direct product of incomplete combustion primarily from biomass and fossil fuel on the surface and a by-product of oxidation of CH${}_{\mathrm{4}}$ and non-methane hydrocarbons in the atmosphere (Brenninkmeijer and Novelli, 2003). Being a precursor to the formation of tropospheric ozone, CO also plays an important role in tropospheric chemistry (Chin et al., 1994). Because of its low background concentration and moderately long lifetime (weeks to months) in the troposphere, CO is an effective tracer for the long-range transport of pollution (Forster et al., 2001) and carbon emissions (Gamnitzer et al., 2006). Nadir observation of CO from space has been providing long-term global coverage from both thermal (TIR) and near-infrared (NIR) instruments. One of the earliest attempts to retrieve atmospheric CO was made by the Interferometric Monitor of Greenhouse gases (IMG) on board the Japanese ADEOS satellite (Barret et al., 2005). From the early 2000s, the Measurements Of Pollution in The Troposphere (MOPITT) instrument on board NASA's Terra satellite launched was the first to provide routine global maps of CO daily (Deeter et al., 2003). Following missions with CO nadir observation capability include the Infrared Atmospheric Sounding Interferometer (IASI) on board Metop-A/B (Hurtmans et al., 2012), the SCanning Imaging Absorption spectroMeter for Atmospheric CHartographY (SCIAMACHY) on board the European ENVISAT satellite (Buchwitz et al., 2005), the Tropospheric Emission Sounder (TES) on board NASA's Aura satellite (Luo et al., 2007) and the Cross-track Infrared Sounder (CrIS) on board the Suomi National Polar-orbiting Partnership platform (Goldberg et al., 2013; Gambacorta et al., 2014). More recently, TROPOMI and GOSAT-2, covering the NIR spectra, have provided additional daily global views of CO (Borsdorff et al., 2018; Noël et al., 2022). However, none of the current instruments and missions provide diurnal CO measurements with high temporal resolution from a GEO platform.

In this study, we report the first result of diurnal CO retrieved from the hyperspectral infrared measurements by the GIIRS using the FengYun Geostationary satellite Atmospheric Infrared Retrieval (FY-GeoAIR) algorithm. The retrieval algorithm uses the absorption feature of CO's fundamental 1–0 rotation–vibration band centered around 4.7 $\mathrm{\mu }\mathrm{m}$ (2150 cm${}^{-\mathrm{1}}$), which allows the measurement to be made during the daytime and the nighttime and provides important vertical information from the retrieval (Crevoisier, 2018). The clear-sky CO retrievals and uncertainties are produced as well as the averaging kernel ($\mathbf{AK}$) matrix for each retrieval that quantifies its vertical observation sensitivity and information content.

This paper is organized as follows. In Sect. 2, the GIIRS instrument and the observed spectra data are introduced. In Sects. 3 and 4, we describe the details of the forward model based on radiative transfer and the inverse model based on optimal estimation theory, respectively. We show results from a simulation experiment in Sect. 5 to assess the performance of the retrieval algorithm. Results of CO retrievals from applying the algorithm to GIIRS spectra in July of 2022 are demonstrated in Sect. 6, followed by discussions and conclusions in Sects. 7 and 8, respectively.

2 The Geostationary Interferometric Infrared Sounder (GIIRS)

2.1 GIIRS

The FY-4 satellites series are China's second-generation geostationary meteorological satellites with improved capabilities for weather and environmental monitoring. FY-4B, the second satellite in the FY-4 series, was launched in June 2021, following FY-4A, which was launched in December 2016. The GIIRS on board FY-4 is an infrared Fourier transform spectrometer based on a Michelson interferometer, also the first space-borne interferometer in geostationary orbit, primarily aiming to measure the three-dimensional atmospheric structure of temperature and water vapor for the numerical weather forecast. FY-4B/GIIRS is located at an altitude of 35 786 km above the Equator at 123.5${}^{\circ }$ E after launch and was relocated to 133${}^{\circ }$ E after 11 April 2022. The observation domain of FY-4B/GIIRS is mostly over eastern Asia, with a focus on China, as shown in Fig. 1a. Maps of surface pressure and temperature, which show large range of variability in the observation domain, are presented in Fig. A1 in Appendix A. FY-4B/GIIRS makes routine observations of the full region every 2 h and 12 times per day (starting at 00:00, 02:00, 04:00,$\mathrm{\dots }$, 22:00 UTC, respectively). Note that the starting hours have been changed to 01:00, 03:00, 05:00,$\mathrm{\dots }$, 23:00 UTC after 6 September 2022. Each full region observation comprises 12 horizontal scans, and each scan sequence consists of 27 fields-of-regards (FORs) plus one deep space (DS) and one internal calibration target (ICT) measurement. The DS and ICT measurements are used as two known radiation sources to radiometrically calibrate the Earth-observing spectra. One full region coverage takes about 1.5 h, and in the following 0.5 h of each 2 h observing cycle, the sounder is operated in the external calibration mode for instrument performance validation. The layout of the 2-dimensional infrared plane array detector for each FOR is shown in Fig. 1b. The detector has $\mathrm{16}\times \mathrm{8}$ pixels with a sparse arrangement. A pixel spans 120 $\mathrm{\mu }\mathrm{m}$ and the field of view (FOV) is 336 $\mathrm{\mu }\mathrm{rad}$. The spatial sampling on the Earth's surface is about 12 km at Nadir. The observed Earth's upwelling infrared radiation covers two spectra regions: long-wave IR band from 680 to 1130 cm${}^{-\mathrm{1}}$ and mid-wave IR band from 1650 to 2250 cm${}^{-\mathrm{1}}$ with a spectral resolution of 0.625 cm${}^{-\mathrm{1}}$. With low instrument noise and a high spectral resolution and range similar to current LEO IR sounders, GIIRS is in principle capable of measuring trace gases, including CO, and providing full day–night diurnal cycle observations. Figure 1c shows an example of GIIRS spectra for the CO retrieval window from 2143 to 2181.25 cm${}^{-\mathrm{1}}$, and the Jacobian for CO and the interference gas H${}_{\mathrm{2}}$O to demonstrate their contribution to the absorption features in the original spectra. In this micro-window, the absorption features from CO and the primary interference gas H${}_{\mathrm{2}}$O are mostly separated and can be distinguished. Examples of Jacobian as a function of pressure and absorption strength are shown in Fig. S1 in the Supplement. The changing Jacobian values demonstrate the vertical sensitivity of the CO absorption lines at different pressure levels, which peak at the surface layer in the daytime and around mid-troposphere in the nighttime.

Figure 1

(a) FY-4B/GIIRS observation coverage from the tropics to $\sim$ 60${}^{\circ }$ N and from $\sim$ 60 to $\sim$ 140${}^{\circ }$ E. The footprints on the left are sparse because of the geometric effect related to the large viewing zenith angle. The color denotes the observed radiance at 2132.5 cm${}^{-\mathrm{1}}$ in 04:00–05:00 UTC on 24 July 2022, as an example. (b) The layout of the 2-dimensional infrared plane array detector of GIIRS. The detector has $\mathrm{16}\times \mathrm{8}$ pixels with a sparse arrangement. A pixel spans 120 $\mathrm{\mu }\mathrm{m}$ and the field of view is 336 $\mathrm{\mu }\mathrm{rad}$. The spatial sampling on the Earth's surface is about 12 km at nadir. (c) (top) An example of GIIRS spectra in the CO retrieval window from 2143 to 2181.25 cm${}^{-\mathrm{1}}$; (bottom) Jacobian at different channels for CO and the interference gas H${}_{\mathrm{2}}$O in the fourth layer, where the averaging kernel value peaks.

[Figure omitted. See PDF]

2.2 Assessment of GIIRS pre-launch instrument noise

For predicting FY-4B/GIIRS's post-launch performance, a series of blackbody calibration experiments have been conducted before launch in a laboratory thermal vacuum tank to evaluate the radiometric performances of the GIIRS instrument. As described in detail by Li et al. (2022), the evaluation results showed that the noise equivalent differential radiance (NedR) on average in the mid-wave IR bands, covering the CO absorption channel, is less than 0.1 mW (m${}^{\mathrm{2}}$ sr cm${}^{-\mathrm{1}}$)${}^{-\mathrm{1}}$. As for the radiometric calibration, the mid-wave IR band is susceptible to noise when the instrument is used to observe low-temperature targets. Nevertheless, the radiometric noise in brightness temperature also met the 0.7 K requirement in the range of 260–315 K, which is comparable to existing infrared sounders. As a result, low instrument noise for GIIRS makes it possible to provide a strong constraint on retrieving CO vertical distribution.

2.3 Filtering of cloudy GIIRS pixels

Only clear-sky or near-clear-sky pixels are considered in the retrieval algorithm. To filter out cloudy pixels, we adopted the higher-resolution (4 km) level-2 cloud mask (CLM) data product from the Advanced Geostationary Radiation Imager (AGRI) on board FY-4B. AGRI uses multispectral threshold algorithms based on different spectral characteristics of VIS, NIR and TIR bands under cloudy and clear conditions to obtain cloud mask information (Lai et al., 2019). The cloud mask of AGRI classifies pixels into four categories: clear, probably clear, probably cloudy and cloudy. We collocated the GIIRS and AGRI footprints and assigned the GIIRS to be clear or near-clear when at least 80 % of the collocated AGRI pixels are labeled as clear or probably clear. For each measurement cycle, there are $\mathrm{12}\times \mathrm{27}$ FORs and each FOR collects $\mathrm{16}\times \mathrm{8}$ observations using the infrared plane array detector. The total is 41 472 observations. For each day with 12 measurement cycle, the total number of observations is about 500 000. After cloud screening and excluding data with viewing zenith angle larger than 70${}^{\circ }$, the average daily number of clear-sky observations is about 90 000 in July 2022.

3 The forward model in FY-GeoAIR for simulating observed spectra

An accurate radiative transfer (RT) model for simulating spectra is a prerequisite for constructing the inversion system for atmospheric composition retrieval. The thermal RT model is built based on radiative transfer theory with inputs of (1) atmospheric state including profiles of temperature, water vapor, atmospheric composition, and surface features; (2) the instrumental specifications, such as instrument spectral response function, and observing geometries; and (3) a spectroscopic database for computing the absorption cross-sections of gas molecules.

3.1 Radiative transfer in the thermal infrared

The upwelling spectral radiance observed by GIIRS can be computed by integrating the RT Eq. (1), which includes the same processes as the forward RT models by TES (Clough et al., 2006) and IASI (Hurtmans et al., 2012). Under clear conditions, scattering by clouds and aerosols can be ignored. For the CO absorption window around 2150 cm${}^{-\mathrm{1}}$, the surface-reflected solar radiation accounts for several percent in the total upwelling radiance and, therefore, cannot be neglected. The upwelling radiance received by a nadir-viewing satellite includes four main components: (a) surface emission (first term on the right-hand side of Eq. 2); (b) upwelling atmospheric emission from the bottom to the top of the atmosphere (second term on the right-hand side of Eq. 1); (c) surface-reflected downwelling atmospheric emission (second term on the right-hand side of Eq. 2); and (d) surface-reflected solar radiation (third term on the right-hand side of Eq. 2). All of these radiation sources are attenuated by the atmosphere. The RT equation is given by

1$$\begin{array}{rl}{I}_{\mathit{\nu }}^{\uparrow }\left(\mathit{\tau }=\mathrm{0},\mathit{\mu }\right)& =I_{\mathit{\nu }}^{\uparrow }\left({\mathit{\tau }}_v^{\ast },\mathit{\mu }\right)\cdot T_{\mathit{\nu }}\left({\displaystyle \frac{{\mathit{\tau }}_v^{\ast }}{\mathit{\mu }}}\right)\\ & +{\int }_{\mathrm{0}}^{{\mathit{\tau }}_v^{\ast }}{B}_{\mathit{\nu }}\left(t\left({\mathit{\tau }}^{\prime }\right)\right)\cdot {\displaystyle \frac{\partial T_{\mathit{\nu }}\left(\frac{{\mathit{\tau }}^{\prime }}{\mathit{\mu }}\right)}{\partial {\mathit{\tau }}^{\prime }}}\mathrm{d}{\mathit{\tau }}^{\prime },\end{array}$$ and $I_{\mathit{\nu }}^{\uparrow }\left({\mathit{\tau }}_v^{\ast },\mathit{\mu }\right)$ is the upwelling radiance from the surface layer comprising three sub-processes given by 2$$\begin{array}{rl}{I}_{\mathit{\nu }}^{\uparrow }\left({\mathit{\tau }}_v^{\ast },\mathit{\mu }\right)& ={\mathit{ϵ}}_{\mathit{\nu }}\cdot B_{\mathit{\nu }}\left(t_{\mathrm{skin}}\right)+\left(\mathrm{1}-{\mathit{ϵ}}_{\mathit{\nu }}\right)\cdot {\stackrel{\mathrm{̃}}{I}}_{\mathit{\nu }}^{\downarrow }\left({\mathit{\tau }}_v^{\ast }\right)\\ & +{\mathit{\alpha }}_{\mathit{\nu }}\cdot I_{\mathit{\nu }}^{\downarrow \odot }\left({\mathit{\tau }}_v^{\ast }\right),\end{array}$$ in which $\mathit{\tau }$ is the optical depth, and $\mathit{\tau }=\mathrm{0}$ and ${\mathit{\tau }}_v^{\ast }$ represent the top and the bottom of the atmosphere, respectively; $\mathit{\mu }$ is the cosine of the satellite viewing zenith angle; $B_{\mathit{\nu }}\left(t\right)$ is the Planck function for computing black-body radiation at temperature $t$; $T_{\mathit{\nu }}\left(\mathit{\tau }\right)$ is the transmission at level $\mathit{\tau }$; ${\mathit{ϵ}}_{\mathit{\nu }}$ is the emissivity; ${\mathit{\alpha }}_{\mathit{\nu }}$ is the surface reflectance; $I_{\mathit{\nu }}^{\downarrow \odot }\left({\mathit{\tau }}_v^{\ast }\right)$ is the solar radiation reaching the surface level; ${\stackrel{\mathrm{̃}}{I}}_{\mathit{\nu }}^{\downarrow }\left({\mathit{\tau }}_v^{\ast }\right)$ is the total downwelling flux reaching the surface, integrated upon all the geometries by considering a Lambertian surface. Similar to Clough et al. (2006) and Hurtmans et al. (2012), the evaluation of this equivalent downward flux integral can be simplified by computing an effective downward radiance with a zenithal angle of 53.51${}^{\circ }$, which gives a very accurate approximation of the integral for emissivity larger than 0.9 (Turner, 2004).

The monochromatic radiances at a high resolution of 0.05 cm${}^{-\mathrm{1}}$ (over-sampled by 12 times compared to GIIRS spectral resolution of 0.625 cm${}^{-\mathrm{1}}$) are simulated and then convolved with the GIIRS instrument line shape (ILS) to obtain calculated radiances at the same resolution as GIIRS that can directly be compared with the GIIRS spectra. ILS for GIIRS is constructed using a standard SINC function with a maximum optical path difference (MOPD) of 0.8 cm. The original spectra are not apodized to retain the original spectral absorption features. Instead, a wide ILS, with a width of 40 cm${}^{-\mathrm{1}}$, is used to account for the contribution from oscillating side lobes on both sides of the SINC function (Gambacorta and Barnet, 2018).

3.2 A priori atmospheric and surface parameters

The RT model in FY-GeoAIR requires inputs of atmospheric state parameters including profiles of temperature, water vapor, and atmospheric composition and surface parameters. The data sources and their specifications are described below.

3.2.1 The a priori CO profile and the associated covariance matrix

Since CO is the primary gas to be retrieved, constructing an appropriate a priori for the retrieval algorithm is important. There are currently two different approaches. One is a fixed a priori CO profile for all retrievals. This approach has been used by IASI CO retrieval algorithm (Hurtmans et al., 2012). A static a priori is found to be more sensitive to unexpected events such as wildfires that lead to high CO emissions, because the variability associated with the a priori profile is larger in the retrieval algorithm (George et al., 2015). The second is spatially and temporally varying a priori CO fields from a model-derived monthly climatology. This approach has been used by the retrieval algorithm of TES (Luo et al., 2007) and MOPITT (Deeter et al., 2010); A climatology-based a priori provides the best a priori knowledge from the model and has been shown to have a better performance over regions with persisting high levels of CO throughout the year, such as urban areas (George et al., 2015).

However, time-varying a priori profiles make the retrieval results more complicated to interpret and to use for model validation, and the smaller variability associated with the a priori also makes it less sensitive to anomalies. Although a variable a prior profile can better capture variability and seasonality at different latitudes, it may not reflect the exact information existed in the observed spectra. For our purpose of retrieving the diurnal changes of CO columns, the main topic of this study, a fixed a priori is preferred because any significant perturbation to the constant a priori, which does not change diurnally, may indicate information that is retrieved from the observed spectra. To construct a fixed a priori profile and the associated covariance matrix, we used the CO simulations from the ECMWF Atmospheric Composition Reanalysis 4 (EAC4) monthly averaged fields (Inness et al., 2019), which have a horizontal resolution of 0.75${}^{\circ }$ $\times$ 0.75${}^{\circ }$, a temporal resolution of 3 h and 25 pressure levels from 1000 to 1 hPa. Data for the year 2021 over the land region are used, except for the Tibetan Plateau region where the CO is constantly low due to its high elevation. Over the ocean, we use the East China Sea only to avoid oversampling of ocean CO profiles. Note that the EAC4 has assimilated MOPITT and IASI retrievals which can capture wildfire information. However, such information has almost completely reduced the resulting a priori profile, which is averaged from a large number of simulated profiles with the majority not affected by wildfire emissions. The mean and 1 standard deviation of the simulated CO profiles are used as the a priori and the associated error, respectively. This fixed a priori profile is used for different time and locations, and no seasonality is assumed. To construct the correlation matrix, we used a correlation length of 3 km based on our analysis using EAC4 reanalysis. The covariance matrix can be calculated based on the a priori error and the correlation matrix. The resulted CO a priori and the associated covariance matrix are shown in Fig. 2. For pressure levels that do not match the values shown in Fig. 2a, interpolation for pressure levels is carried out. Although the forward radiative transfer model (Sect. 3.2.4) has a full 47-layer atmosphere from 1000 to 1 hPa, we only retrieve the layers below 200 hPa and keep the layers above as the a priori.

Figure 2

(a) The a priori CO profile in volume mixing ratio from surface to about 200 hPa. The 12 levels corresponds to 11 layers, and each layer has a thickness of about 1 km; (b) the associated covariance matrix in unitless multiplicative factor for the 12 levels in panel (a). In the retrieval algorithm, only the layers below 200 hPa are retrieved while keeping the layers above as the a priori.

[Figure omitted. See PDF]

3.2.2

Atmospheric profiles of H${}_{\mathrm{2}}$O, CO${}_{\mathrm{2}}$, N${}_{\mathrm{2}}$O and O${}_{\mathrm{3}}$

In the spectral window from 2143 to 2181.25 cm${}^{-\mathrm{1}}$, the interference gases include H${}_{\mathrm{2}}$O, CO${}_{\mathrm{2}}$, N${}_{\mathrm{2}}$O and O${}_{\mathrm{3}}$. H${}_{\mathrm{2}}$O and O${}_{\mathrm{3}}$ are extracted from the ECMWF ERA5 reanalysis (Hersbach et al., 2020), which has a horizontal resolution of 0.25${}^{\circ }$ $\times$ 0.25${}^{\circ }$, a temporal resolution of 1 h and 37 pressure levels from 1000 to 1 hPa. N${}_{\mathrm{2}}$O and CO${}_{\mathrm{2}}$ are extracted from ECMWF CAMS global inversion-optimized greenhouse gas fluxes and concentrations (ECMWF, 2022), which have a spatial resolution of 1.9${}^{\circ }$ $\times$ 3.75${}^{\circ }$, a temporal resolution of 3 h and 39 pressure levels from 1000 to 1 hPa. The latest available years of datasets in 2019 for N${}_{\mathrm{2}}$O and 2021 for CO${}_{\mathrm{2}}$ are used.

3.2.3 Atmospheric temperature profile

The atmospheric temperature profile is a key input in the forward RT model for computing the blackbody emission by the atmosphere. The atmospheric temperature data are extracted from the ECMWF ERA5 reanalysis (Hersbach et al., 2020), which has a horizontal resolution of 0.25${}^{\circ }$ $\times$ 0.25${}^{\circ }$, a temporal resolution of 1 h and 37 pressure levels from 1000 to 1 hPa.

3.2.4 Surface emissivity, surface skin temperature and surface pressure

Surface emissivity and skin temperature are important parameters in computing surface blackbody emission. For the surface land data, we used the global infrared land surface emissivity database from the University of Wisconsin – Madison (UOW-M) (Seemann et al., 2008). The dataset has 10 bands in wavenumber, ranging from mid-wave infrared to long-wave infrared. Interpolation is performed to derive the emissivity in the CO channels. For ocean surface emissivity, we adopted the ocean emissivity model, which is a function of viewing zenith angle and wind speed, from Masuda et al. (1988). Surface skin temperature and surface pressure are extracted from ERA5 hourly data on a single level (Hersbach et al., 2020), which has a spatial resolution of 0.25${}^{\circ }$ $\times$ 0.25${}^{\circ }$. The surface pressure from the ECMWF reanalysis has a typical accuracy of 2–3 hPa (O'Dell et al., 2012).

The number of pressure grids in the forward RT model should be large enough to reduce the error associated with the discretization of the atmosphere (Clough et al., 2006). Here we define a 47-layer target atmosphere with an equal thickness of about 1 km from 1000 to 1 hPa. All the above-described atmospheric a priori profiles are interpolated to the target pressure grids. The pressure grids are kept fixed except for the surface level which is determined by the surface pressure.

3.3 Spectroscopic database: look-up tables of absorption cross-section

Deriving the absorption optical depth of gas molecules for the RT model would require the line-by-line calculation of absorption cross section based on spectroscopic line parameters and line shape. However, this line-by-line calculation at high spectral resolution for a wide spectral window is computationally expensive. Instead, to speed up the calculation, absorption coefficient (ABSCO) for different molecules at different pressures and temperatures are precalculated and stored in lookup tables (LUTs). For gas absorptions that have H${}_{\mathrm{2}}$O dependence, the ABSCO dependence on H${}_{\mathrm{2}}$O is also considered. This method of building ABSCO lookup tables has been adopted in previous retrieval algorithms, including the FORLI for IASI (Hurtman et al., 2012) and the ELANOR for TES (Clough et al., 2006).

In this study, ABSCO LUTs are built using the extensively validated Line-By-Line Radiative Transfer Model (LBLRTM v12.11; Clough et al., 2005). LBLRTM uses the HITRAN database as the basis for line parameters. These line parameters from HITRAN, plus additional line parameters from other sources, are combined for LBLRTM by a line file creation program called LNFL (v3.2). In addition to modeling individual spectral lines and absorption cross-sections, LBLRTM also takes into account the H${}_{\mathrm{2}}$O, CO${}_{\mathrm{2}}$, O${}_{\mathrm{2}}$ and N${}_{\mathrm{2}}$ continua in the thermal infrared using the MT_CKD continuum database (MT_CKD_3.4). The self-broadening absorption of H${}_{\mathrm{2}}$O nonlinearly depends on its concentration which should be considered for calculating H${}_{\mathrm{2}}$O ABSCO. It has been shown that the dependence is nearly linear for a given temperature and pressure. Therefore, to account for this effect in the LUT, we computed the H${}_{\mathrm{2}}$O ABSCO at two H${}_{\mathrm{2}}$O volume mixing ratio (VMR) values: 1 ppm (dry air) and $\mathrm{4}\times {\mathrm{10}}^{\mathrm{4}}$ ppm (wet air). The ABSCO values at other H${}_{\mathrm{2}}$O values can be calculated by linear interpolation. In LBLRTM, the line-by-line calculation resolution is set to be $\mathrm{2.0}\times {\mathrm{10}}^{-\mathrm{4}}$ cm${}^{-\mathrm{1}}$ and later integrated into the ABSCO LUT table resolution at $\mathrm{5.12}\times {\mathrm{10}}^{-\mathrm{2}}$ cm${}^{-\mathrm{1}}$, which is oversampled by about 10 times compared to the GIIRS resolution of 0.625 cm${}^{-\mathrm{1}}$. The LUTs are built for 49 atmospheric pressure levels from 1025 to 1 hPa with a pressure step equivalent to 1 km and 15 temperatures from 180 to 320 K with a step of 10 K.

4 Retrieval algorithm in FY-GeoAIR based on optimal estimation theory

The goal of the retrieval algorithm for retrieving CO from nadir-viewing instruments based on optimal estimation theory is to find a solution for the state vector, which consists of CO profile and auxiliary parameters, such that the RT simulations best fit the measured spectra. The optimal estimation method has been described thoroughly in Rodgers (2000) and applied in several previous studies by the group (Zeng et al., 2017, 2021; Natraj et al., 2022).

4.1 Atmospheric inversion based on optimal estimation

The goal of optimal estimation is to find the solution for the state vector that minimizes the following cost function (Rodgers, 2000):

3$$\begin{array}{rl}J\left(\mathit{x}\right)& ={\mathit{\chi }}^{\mathrm{2}}={\left[\mathit{y}-\mathbf{F}\left(\mathit{x},\mathit{b}\right)\right]}^T{{\mathbf{S}}_{\mathit{\epsilon }}}^{-\mathrm{1}}\left[\mathit{y}-\mathbf{F}(\mathit{x},\mathbf{b})\right]\\ & +{\left(\mathit{x}-{\mathit{x}}_{\mathrm{a}}\right)}^T{\mathbf{S}}_{\mathrm{a}}^{-\mathrm{1}}(\mathit{x}-{\mathit{x}}_{\mathrm{a}}),\end{array}$$ where $\mathit{y}$ is the observed GIIRS spectral radiance at the CO retrieval window from 2143 to 2181.25 cm${}^{-\mathrm{1}}$, which is found to be the best window that minimizes interferences by other gases while maximizing the information content for CO retrieval (De Wachter et al., 2012); $\mathit{x}$ is the state vector consisting a set of parameters to be retrieved, including CO profile, H${}_{\mathrm{2}}$O profile, surface skin temperature and atmospheric temperature profiles. Of the 47-layer atmosphere defined in the forward model, the algorithm only retrieves layers below 200 hPa (in total of 11 layers at maximum) and uses the a priori for the layers above. $\mathbf{F}$ is the forward RT model for simulating radiance as introduced in Sect. 3; $\mathit{b}$ is a set of model parameters in the RT model that are not retrieved, such as profiles of interference gases (O${}_{\mathrm{3}}$, CO${}_{\mathrm{2}}$ and N${}_{\mathrm{2}}$O), surface emissivity and other relevant geophysical parameters. $\mathit{\epsilon }$ is the spectral error vector containing the noise in the spectra observation. ${\mathbf{S}}_{\mathit{\epsilon }}$ is the measurement error covariance matrix; ${\mathit{x}}_{\mathrm{a}}$ is the a priori state vector; ${\mathbf{S}}_{\mathrm{a}}$ is the a priori covariance matrix for the state vector. For simplicity in calculating ${\mathbf{S}}_{\mathit{\epsilon }}$, we assume that the measurement noise dominates and there is no cross-correlation between different spectral channels, resulting in a diagonal matrix. The instrument noise (NedR) for each spectral observation, as described in Sect. 2.2, is used as the measurement noise. A commonly used statistic for quantifying the goodness of fit is the reduced ${\mathit{\chi }}^{\mathrm{2}}$, which is computed as the cost function value after convergence divided by the degree of freedom, which is the number of channels in the absorption window (which is 64) minus the number of elements in the state vector (which is 4). After evaluating the reduced ${\mathit{\chi }}^{\mathrm{2}}$ from test runs, we found that the value on average is systematically lower than the theoretical mean value of 1.0, indicating that the measurement error may have been underestimated. Therefore, in this study, we enlarge the measurement noise by 1.5 times such that the averaged reduced ${\mathit{\chi }}^{\mathrm{2}}$ value from the retrievals is close to 1.0. The extra noise added may represent the uncertainty from the forward model, spectroscopy and the forward model inputs, which are not accounted for by the original instrument noise alone. ${\mathbf{S}}_{\mathrm{a}}$ is a very important parameter that should not be too tight or loose to provide a suitable constraint on the retrieval. It can be calculated based on the error in CO a priori profile and the correlation matrix derived from model simulations, as described in Sect. 3.2.1. To obtain the solution for Eq. (3), we adopt the Levenberg–Marquardt method (Rodgers, 2000) to find the optimal estimate of $\mathit{x}$.

4.2

Averaging kernel ($\mathbf{AK}$) matrix and degree of freedom for signal (DOFS)

The quality of the retrieval can be characterized by two quantities: the $\mathbf{AK}$ matrix and the DOFS. $\mathbf{AK}$ matrix is an important statistical metric for describing the sensitivity of the retrieval to the true state by the current observing system. The full averaging kernel matrix ($m\times m$) is given by 4$$\mathbf{A}={\left({\mathbf{K}}^T{{\mathbf{S}}_{\mathit{\epsilon }}}^{-\mathrm{1}}\mathbf{K}+{\mathbf{S}}_{\mathrm{a}}^{-\mathrm{1}}\right)}^{-\mathrm{1}}{\mathbf{K}}^T{{\mathbf{S}}_{\mathit{\epsilon }}}^{-\mathrm{1}}\mathbf{K},$$ where $m$ is the number of atmospheric layers. $\mathbf{K}$ is the Jacobian matrix, which is the first derivative of the forward model with respect to the state vector. $A_{ij}$ represents the derivative of the retrieved CO at level $i$ with respect to the true CO at level $j$, representing a relative contribution of the true state to the retrieved state. An ideal observing system would produce an $\mathbf{AK}$ matrix close to the identity matrix, meaning the observations are sufficiently good to constrain each element in the retrieval vector. In reality, the $\mathbf{AK}$ can be very different from an identity matrix, meaning that the information from the true state is smoothed vertically over different layers by the retrieval algorithm. The rows of $\mathbf{AK}$ can be regarded as smoothing functions. The trace of the $\mathbf{AK}$ matrix, representing the number of independent elements of information extracted by the retrieval algorithm from the measurement, quantifies the DOFS. It is an important concept in describing the vertical resolution of the retrieval profile. For example, a DOFS of 1 means that at least one independent piece of information on the vertical distribution of CO can be retrieved from the spectral measurement.

4.3 Post-processing

All cloud-screened GIIRS spectra acquired over land and ocean at solar zenith angle less than 70${}^{\circ }$ are used in the retrieval. In the post-processing, multiple filters are applied to ensure good retrieval quality. First, retrievals that fail to converge after 10 iterations are excluded. Second, retrievals with the goodness of fit, quantified by reduced ${\mathit{\chi }}^{\mathrm{2}}$, less than 1.5 are excluded. Lastly, retrievals with root-mean-square error of the fitting brightness temperature (BT) residual that are more than 1 standard deviation away from the mean, which is about 0.7 K in July 2022, are excluded. After data screening, the total number of observations in July 2022 (in total 2 812 071) is reduced to 2 045 228.

5 Inversion experiments using simulated synthetic spectra

The goal of applying the FY-GeoAIR algorithm to simulated synthetic spectra is to assess the performance of the algorithm in retrieving CO profiles and to quantify the impacts on the accuracy due to the spatially and temporally varying thermal contrast (TC) in eastern Asia. TC is defined as the temperature difference between the surface and the lower atmospheric layer (Clarisse et al., 2010), and it is found to be a key indicator of the information content for retrieving CO profile, especially the lower-tropospheric CO, from infrared thermal radiance.

Four representative regions are specially selected for inter-comparisons, including (1) North China Plain (covering 32–40${}^{\circ }$ N and 114–120${}^{\circ }$ E), which represents industrialized urban regions with persistently high CO emissions in China; (2) Mongolia (covering 42–50${}^{\circ }$ N and 100–115${}^{\circ }$ E), which represents CO background regions; (3) the East China Sea (covering 25–33${}^{\circ }$ N and 122–129${}^{\circ }$ E), which represents ocean surface; and (4) northern India (23–28${}^{\circ }$ N and 75–83${}^{\circ }$ E), which represents industrialized urban regions in India. The locations of these regions are shown in the Appendix Fig. A1a. The diurnal changes of surface temperatures and bottom air temperatures, as shown in Fig. 3a, show distinctive patterns over these selected regions. Compared to the atmosphere, Earth's surface, especially over land, heats up and cools down more quickly because of its relatively low heat capacity. This mechanism results in a larger diurnal variation for the surface than for the atmosphere: TC is thus more pronounced during the day than the night. Specifically, the East China Sea has a relatively flat change, as expected for ocean water due to its large heat capacity and ocean water mixing; the Mongolia region, covered by a mixture of grass and bare land, has the largest diurnal change; the North China Plain and northern India, surrounded by urban clusters with a mixture of residential and agriculture lands, have a moderate diurnal change. The complexity of the diurnal TC change as demonstrated by various land use types in eastern Asia affects the diurnal changes of DOFS from the CO retrievals by FY-4B/GIIRS, as shown in Fig. 3b. TC is significantly correlated with the DOFS from the CO retrievals for both the total column and the lower atmospheric partial column (the bottom three layers in this case). A higher TC in the daytime results in a larger DOFS. The information content for the lower atmosphere shows a similar pattern to the total column but a larger relative change between daytime and nighttime. A similar relationship can be found in LEO satellites (e.g., Bauduin et al., 2017).

Figure 3

(a) The diurnal change of surface temperature and bottom two-layer mean air temperature extracted from ECMWF ERA5 reanalysis data for the four representative regions: North China Plain, Mongolia, East China Sea and northern India. These temperature values are averaged for every 2 h corresponding to the clear-sky GIIRS observations in July 2022. (b) The diurnal change of DOFS for the total column and the bottom three-layer (from the surface to 3 km a.s.l.) atmosphere. The error bars represent regional data variabilities. BJT represents Beijing time (UTC$+$8).

[Figure omitted. See PDF]

The synthetic spectra are generated using the same forward RT model as described in Sect. 3, except that we use the original ECMWF EAC4 3-hourly simulated CO as the “truth” and add Gaussian white noise with mean of zero and a standard deviation equal to NedR $\times \mathrm{1.5}$. Since we assume no error in the forward RT model, the spectra error solely comes from the added noise. The retrieval algorithm is then applied to these synthetic spectra using the fixed a priori CO as described in Sect. 3.2. The retrievals are compared with the “truth” to investigate the impacts of TC and $\mathbf{AK}$ on their differences.

To evaluate the performance of the retrieval algorithm, we compare (1) the retrievals and the “truth” and (2) the a priori and the “truth”. The comparisons in North China Plain are shown in Fig. 4, while the comparisons in Mongolia, East China Sea and northern India are shown in Figs. S2, S3 and S4, respectively. From Fig. 4, we can see that the retrieved CO total columns have a higher correlation with the “truth” than with the a priori column. Note that the small variation of the a priori column derived from the fixed a priori profile is caused by the surface pressure difference within the region. The comparison suggests that the retrieval algorithm is effective and the observed spectra are providing useful information to constrain the CO profiles. In the daytime, when the DOFS is higher, the retrieved CO columns show the largest correlation and the smallest bias when compared with the “truth” columns. In the nighttime, however, DOFS becomes smaller, especially in the lower atmosphere. This low DOFS means that the CO profile retrievals are under-constrained and show a larger bias when compared with the “truth” columns. The information for the bottom-layer CO may be extrapolated from the free troposphere (Bauduin et al., 2017; George et al., 2015). This information extrapolation may lead to a higher bias in the retrieval for the bottom-layer CO. Overall, we can conclude that a higher (lower) TC leads to a higher (lower) DOFS for the retrieval, which in turn contributes to a smaller (larger) bias in the retrieval.

Figure 4

Results from inversion experiments in North China Plain. Left: comparison between CO a priori total column and CO column “truth”; middle: comparison between CO total column retrieval and CO column “truth”, and right: comparison between CO total column retrieval and the “truth” after $\mathbf{AK}$ smoothing. These results are from synthetic simulation experiments using data on 7 and 24 July 2022. The results are shown for every 4 h. BJT represents Beijing time (UTC$+$8). Results from inversion experiments for Mongolia, East China Sea and northern India are shown in the Supplement.

[Figure omitted. See PDF]

Since the sensitivity of the CO retrieval is pressure dependent, we implement a profile correction by applying the GIIRS $\mathbf{AK}$ to smooth the “truth” profile, to account for the different resolution between the retrieval and the “truth” (Rodgers and Connor, 2003): 5$${\mathrm{CO}}_{\mathrm{true}}^{\mathrm{AKcorrect}}={\mathrm{CO}}_{\mathrm{a}}+\mathbf{A}\cdot \left({\mathrm{CO}}_{\mathrm{true}}-{\mathrm{CO}}_{\mathrm{a}}\right),$$ where $x_{\mathrm{true}}^{\mathrm{AKcorrect}}$ is the smoothed “truth” profile, and $x_a$ and $\mathbf{A}$ are the a priori profile and $\mathbf{AK}$ matrix, respectively, from the GIIRS retrieval. The result is shown in the third column in Fig. 4. The correlations are significantly improved, justifying the use of $\mathbf{AK}$ matrix smoothing for the CO profile from model simulations that have uniform vertical sensitivity. For example, if the model simulation data are close to the “truth”, then after the $\mathbf{AK}$ matrix smoothing, the corrected data should be in high agreement with our GIIRS retrievals.

6 Characteristics of CO retrievals from GIIRS

All cloud-screened GIIRS spectra acquired over land and ocean with viewing zenith angle less than 70${}^{\circ }$ are used in the FY-GeoAIR retrieval algorithm. The retrieval results have been post-screened by the filters described in Sect. 4.3. In this section, we describe the characteristics of the CO retrievals, including the goodness of spectral fitting, DOFS and vertical sensitivity using $\mathbf{AK}$ matrix, and accuracy assessment by comparison with IASI CO retrievals.

6.1 Statistics for spectral fitting

The goodness of spectral fitting is evaluated by two statistics: the spectral fitting residual and the reduced ${\mathit{\chi }}^{\mathrm{2}}$. The latter measures how large the spectral fitting residual compared to spectral noise is. The histogram of the reduced ${\mathit{\chi }}^{\mathrm{2}}$ and the averaged fitting residuals for all the retrievals in July 2022 are shown in Fig. 5. The reduced ${\mathit{\chi }}^{\mathrm{2}}$ shows an expected distribution centering around 1.0. In the post-processing step, we filter the values that are larger than 1.5. The choice of the threshold may vary; here we chose 1.5 to retain more good-quality data while removing retrievals that have an unsatisfactory fitting. The spectral fitting errors in BT show no significant bias. However, a systematic pattern that is persistent among observations at different hours can be seen from the averaged fitting residual from all spectra. However, this pattern is not correlated with the absorption feature of the target gas CO or the primary interference gas H${}_{\mathrm{2}}$O (Fig. 1c). This suggests that the CO spectroscopy adopted from LBLRTM which has undergone extensive verifications is accurate for the purpose of this study. The standard deviations of fitting errors are very consistent across different channels, which is about 0.6 K for the BT error. This suggests that the majority of the channels have fitting errors of less than 1 K. This result is consistent with the pre-launch assessment as described in Sect. 2.2 and Li et al. (2022).

Figure 5

Statistics from spectral fitting. (a) The histogram of reduced ${\mathit{\chi }}^{\mathrm{2}}$ for spectral fitting from all retrievals. (b) The upper panel shows an example of the observed spectra in brightness temperature. The lower panel shows the spectral fitting residual in brightness temperature averaged over all post-screened retrievals in July 2022. The standard deviations of the fitting errors are consistent across different channels, which is about 0.6 K.

[Figure omitted. See PDF]

6.2 Information content analysis

The information content of FY-4B/GIIRS retrievals is assessed by using the $\mathbf{AK}$ matrix and DOFS. The $\mathbf{AK}$ matrix represents the sensitivity of the retrieved state to the true state, in which the matrix row represents how a specific retrieved state vector element reacts to true changes of the state vector at different layers. In the case of the CO profile, for each retrieved layer, the $\mathbf{AK}$ peaks at the altitude containing most information about the profile. The $\mathbf{AK}$ thus provides an estimation of the altitude of maximum sensitivity. Figure 6 shows examples of $\mathbf{AK}$ rows from two different scenarios of TC: higher TC in the daytime (TC $=\mathrm{8.4}$ K) and low TC in the nighttime (TC $=\mathrm{1.0}$ K). The distinctive difference in the lower-tropospheric $\mathbf{AK}$ values demonstrates the importance of high TC in providing information to the lower tropospheric CO retrievals. For the low TC scenario, little information is available from the lower troposphere and the altitude with maximum sensitivity is located around 500 hPa ($\sim \mathrm{5}$ km a.s.l.). In such a case, the information for CO in the lower troposphere is thus extrapolated from the mid-troposphere, which may lead to high bias for the lower troposphere estimate. Figure 7 shows that the diurnal (every 2 h) change of $\mathbf{AK}$ diagonal elements in North China Plain, Mongolia, East China Sea and northern India averaged over all days in July of 2022. The diurnal changes are primarily driven by the changes in TC as shown in Fig. 8. As the TC increases and peaks in the afternoon, the $\mathbf{AK}$ diagonal value increases, and the layer with the maximum moves closer to the surface. In contrast, the East China Sea region has little change among different hours because the TC is relatively flat throughout the day. These results demonstrate that the TC is significantly correlated with the vertical structure of $\mathbf{AK}$ rows from FY-4B/GIIRS retrievals.

Figure 6

Examples of averaging kernel rows from two different scenarios of TC: (a) high thermal contrast in the daytime (TC $=\mathrm{8.4}$ K) and (b) low thermal contrast around Beijing in the nighttime (TC $=\mathrm{1.0}$ K). These are the same two data points in the above figure (in the Supplement).

[Figure omitted. See PDF]

Figure 7

Diurnal (every 2 h) change of averaging kernel diagonal elements in North China Plain, Mongolia, East China Sea and northern India averaged over all days in July 2022. The hour information is based on Beijing time (UTC$+$8).

[Figure omitted. See PDF]

Figure 8

The diurnal changes (every 2 h) of the DOFS mean and standard deviations for (solid) CO total column and (dashed) the bottom three-layer (from the surface to 3 km a.s.l.) partial column in the four representative regions: North China Plain, Mongolia, East China Sea and northern India. These data are averaged over all days in July 2022.

[Figure omitted. See PDF]

DOFS represents another important metric for information content from FY-4B/GIIRS spectra. It quantifies the amount of independent information available from the measurement. Figure 8 shows the diurnal changes of the DOFS mean and standard deviation in the four representative regions averaged over all days in July 2022. In general, the diurnal changes of DOFS track the TC changes over these regions (Fig. 2). Interestingly, we see that the North China Plain and northern India have comparable or higher DOFS to Mongolia, although the latter has a significantly larger TC. This is because, besides TC, the high CO concentration in North China Plain and northern India has a positive contribution to the DOFS, as also shown by Bauduin et al. (2017).

To investigate the relationship between TC and DOFS, the DOFS from the retrievals as a function of TC for the CO total column and bottom three-layer CO partial column for the four representative regions are plotted in Fig. 9. The DOFS for the majority shows a monotonic change with TC. However, for retrievals with negative TCs, the DOFS may increase as the TC becomes more negative. This pattern is consistent with findings by Bauduin et al. (2017), which showed that large negative TC values allow the decorrelation between the low and the high troposphere by capturing the emission of radiation from the lower troposphere. Overall, the DOFS for the total CO column retrieval is between 0.8 and 1.5 for the majority, with a mean value around 1.1, meaning that more than one independent piece of information is retrieved from FY-4B/GIIRS spectra. For the bottom three layers ranging from the surface to 3 km a.s.l., the DOFS for the majority is between 0 and 0.8. The highest DOFS exists over the land region with the largest TC. Similarly, for the DOFS for the bottom three layers, increasing the TC value favors the sensitivity to surface CO.

Figure 9

DOFS from the retrievals as a function of TC for CO total column (left) and bottom three-layer (from the surface to 3 km a.s.l.) CO partial column (right) for the three representative regions: (a) North China Plain and (b) Mongolia, (c) the East China Sea and (d) northern India.

[Figure omitted. See PDF]

6.3 Temporal and spatial variations of CO total column and the DOFS from retrieval

The diurnal changes of CO columns from FY-4B/GIIRS retrievals may be linked to (a) the real CO column variabilities, the objective of this study, primarily driven by emissions, atmospheric transport, and changes in boundary layer height, and (b) the change in instrument detectivity as quantified by the retrieval DOFS that is affected by TC and CO abundance. As an attempt to disentangle these different factors, in Fig. 10 we show the diurnal changes of the CO column retrievals from FY-4B/GIIRS, the boundary layer height (BLH) from ECMWF reanalysis data and the model CO simulations from EAC4 reanalysis over the selected regions. From the model simulations, which has assimilated satellite observations of IASI and MOPITT, we see the change in total columns in all selected regions is very small (less than 2 % on average), which can be primarily attributed to the diurnal change in BLH. In Fig. S6, the model-simulated ground-level CO concentrations show a much larger variation compared to the CO columns. However, model simulations from EAC4 have large grids (0.75${}^{\circ }$ $\times$ 0.75${}^{\circ }$) and low temporal resolution (3 h), which are not sufficient to resolve the local CO changes that are usually measured over the urban central areas. To the first order, the change in the ground-level CO concentration averaged over the selected region is primarily driven by the BLH change, and the traffic emission peaks are not discernable from the time series.

In urban regions, ground level CO concentrations from in situ ground-based observations show a distinctive double-peak diurnal cycle corresponding to the morning and evening traffic rush hours. In the morning, the increase in traffic emissions results in the morning peak; as BLH gets larger, air dilution takes place and the concentration drops. In the evening, traffic emissions increase while the BLH quickly decreases, which results in an evening peak. These diurnal patterns have been observed cross many cities in Asia (e.g., Ran et al., 2009; Chen et al., 2020; Meng et al., 2009; Verma et al., 2017). However, the diurnal changes of CO columns and the surface layer concentration are not expected to be the same. As shown in the study by Stremme et al. (2009), which retrieved diurnal CO column changes in Mexico City using ground-based solar and lunar infrared spectroscopy, it was found that the diurnal changes in the total CO column and the surface level concentration can be very different. The total CO column within the city presents large variations with contributions from urban CO emissions at the surface and the transport of cleaner or more polluted air masses into the study area.

The diurnal cycle of the retrieved CO columns from FY-4B/GIIRS, shown in Fig. 10a, presents impacts by the diurnal change of DOFS. Note that the a priori CO columns averaged for the year of 2021 are 0.038, 0.028, 0.039 and 0.036 mol m${}^{-\mathrm{2}}$, respectively, for the North China Plain, Mongolia, East China Sea and northern India. Since the DOFS for the nighttime is low, especially for the lower atmosphere, the nighttime column retrievals generally tend to close to the a priori columns, resulting in a bow shape. In the daytime, the CO column retrievals are well constrained by the observations. Since the summertime CO is generally lower than the yearly mean (Chen et al., 2020) based on CO's seasonal cycle, we see the column retrievals averaged in July are generally lower than the a priori column value which is derived from annual mean of model simulations. These results suggest that a direct interpretation of the authentic diurnal column variabilities from the retrieved CO columns is challenging given the entangled effects of the real CO changes and the variable detectivity. A better solution is to use mode assimilation (e.g., EAC4) that takes into account the retrieved CO profile and the vertical sensitivity in order to disentangle the different contributions.

Figure 10

(a) The diurnal changes (every 2 h) of the retrieved CO columns averaged over all days in July 2022. The $x$-axis values are slightly shifted intentionally to avoid the overlapping of the error bars. Note that no data are available in hour 23 for the Mongolia region; (b) the diurnal changes (every hour) of averaged boundary layer height in the representative regions in July 2022. The data are averaged from the ECMWF ERA5 boundary layer height reanalysis data; (c) the diurnal changes (every 3 h) of simulated CO columns in the upper panel and the normalized values in the lower panel. The simulation data are averaged from the ECMWF EAC4 reanalysis dataset in July 2021. The recent 2022 data are not available at this point. The error bars in panel (a) and (b) represent day-to-day variabilities. The error bars for panel (c) are too large and therefore not shown.

[Figure omitted. See PDF]

We further compare the diurnal changes of the spatial distribution of (1) the column retrievals and (2) the DOFS values for both the total column and the bottom three-layer partial column. The CO total column and the DOFS from the retrieval algorithm are averaged for every measurement cycle (2 h duration) by aggregating the data from all days in July 2022 into 0.5${}^{\circ }$ $\times$ 0.5${}^{\circ }$ grids. Note that the GIIRS completes a measurement cycle in about 2 h, so the data at a certain location are just an instantaneous value within the measurement cycle. Since CO is a relatively long-lived gas, we can assume the CO values are unchanged during the 2 h period. In total, 12 full domain measurement cycles in eastern Asia are available for every 2 h. Here, we only show every other measurement cycle as examples, in total six full domain measurements for 00:00–02:00, 04:00-06:00, 08:00–10:00, 12:00–14:00, 16:00–18:00 and 20:00–22:00 UTC. The results are shown in Figs. 11a and 12a for the CO total column retrievals. The CO columns have small changes in a day and the spatial pattern is very persistent. Overall, the spatial distribution of the CO total column shows expected spatial patterns, with high values clustered in industrialized urban regions in northern and eastern China, the Sichuan Basin in central China, and northern India. Over the ocean, the enhancement caused by the eastern Asian outflow (Heald et al., 2003) can be observed. In addition, elevated CO column values can be detected around the Siberia region, which is close to the northeastern region of our study area. The high CO values are related to the wildfire emissions over the region, which intensifies in the summer season.

Figure 11

(a) Maps of retrieved CO total columns from FY-4B/GIIRS for hours 0–1 (upper), hours 4–5 (middle) and hours 8–9 (lower) in Beijing time (BJT; UTC$+$8). The CO total columns are monthly averages in July of 2022 that have been re-gridded into 0.5${}^{\circ }$ $\times$ 0.5${}^{\circ }$ grids, (b) the distribution of DOFS for the CO total column and (c) the distribution of DOFS for the CO partial column of the bottom three layers (from the surface to 3 km a.s.l.).

[Figure omitted. See PDF]

Figure 12

The same as Fig. 10 but for hours 12:00–13:00 (upper), hours 16:00–17:00 (middle) and hours 20:00–21:00 (lower) in Beijing time.

[Figure omitted. See PDF]

To evaluate the information content that is available in constraining the CO total column and the bottom three-layer partial column, the maps of the DOFSs are also shown in Fig. 11b, c and 12b, c. In the daytime, when TC is high, the DOFS values over land, especially over eastern and northern China, are higher than 1.0, suggesting that the GIIRS spectra provide more than one piece of independent information to the retrieval. In the nighttime, when the land region cools down quickly and the ocean surface is still warm, a larger TC over the ocean leads to a higher DOFS compared to the land region. A similar pattern can be observed in the DOFS for the bottom three layers, but with smaller DOFS values. Not surprisingly, the DOFS for the bottom three layers also shows a local pattern as the CO emissions (e.g., in northern China). This is because the DOFS from the retrieval is also affected by the CO concentration besides TC, as discussed in Bauduin et al. (2017).

6.4 Accuracy assessment by comparison with IASI CO retrievals

Different from FY-4B/GIIRS, IASI on board Metop-B, which was launched in 2012, is a sun-synchronous polar-orbiting infrared spectrometer designed to measure the upwelling spectral radiance in the infrared using a nadir viewing geometry, with Equator crossing times at 10:30 and 22:30 LT, respectively, in the morning and evening. IASI has a dedicated CO retrieval algorithm (Hurtmans et al., 2012) that was improved over time and has benefited from cross-comparisons with other products (e.g., George et al., 2009; De Wachter et al., 2012; Worden et al., 2013; George et al., 2015). Therefore, a comparison would shed light on the difference between GIIRS infrared CO retrievals and the state-of-the-art retrievals from IASI. In this section, we carry out the spatial and temporal comparisons using publicly available CO from IASI/Metop-B.

For the spatial comparison, we use the daytime and nighttime observations on 7 July 2022 as examples. The observation hours of IASI (Fig. S7) over the North China Plain are about 09:40 BJT for the daytime and 21:00 BJT for the nighttime, which correspond to the GIIRS measurement cycles of 10:00–11:00 and 20:00–21:00 BJT, respectively, for the daytime and nighttime. Because the GIIRS and IASI have different footprints and grid configurations, it is not straightforward to make point-by-point comparisons. We re-grid the retrieval data into 0.5${}^{\circ }$ $\times$ 0.5${}^{\circ }$ grids and then make comparisons of the collocated grid data points. The results are shown in Fig. 13. We can see the spatial distribution of CO columns in the daytime is characterized by two source regions: the North China Plain as a source of anthropogenic emissions and the Siberia region as a source of natural wildfire emissions. This wildfire over Siberia on 7 July 2022 is further confirmed using MODIS optical images and fire counts (not shown here). In the nighttime, the emissions from North China Plain persist. However, the wildfire regions are not covered. The scatter plots comparing the collocating observations show good agreements between the two datasets.

Figure 13

Comparing CO column retrievals from GIIRS (a, d) and IASI (b, e) on 7 July 2022, using daytime (upper panels) and nighttime (lower panels) retrievals. The observation hours are also indicated. The scatter plots (c, f) show the comparison between GIIRS and IASI original and adjusted column data. The adjusted CO column data are generated by adjusting the GIIRS CO retrievals based on the IASI a priori CO profile.

[Figure omitted. See PDF]

When comparing datasets from different instruments, data corrections including an a priori adjustment and an $\mathbf{AK}$ smoothing are usually necessary to account for the difference in the a priori and $\mathbf{AK}$ (Rodgers and Connor, 2003). Fortunately, we found that the DOFS and the vertical sensitivity, as indicated by the $\mathbf{AK}$ diagonal elements, are similar between GIIRS and IASI, as shown in Figs. A2 and S8. The DOFSs from both the daytime and nighttime retrievals are highly correlated although IASI DOFSs are higher by about 10 %. The $\mathbf{AK}$ diagonal profiles from the examples shown in Fig. A2c and d are comparable between GIIRS and IASI for the lower atmosphere, which accounts for the majority of the total column. We therefore assume that both sensors have similar vertical sensitivity. Therefore, only the GIIRS data adjustment based on IASI's a priori CO profile is carried out. We adjust the GIIRS CO retrieval profile $\left({\mathrm{CO}}_{\mathrm{ret}}^{\mathrm{GIIRS}}\right)$ to the IASI a priori profile $\left({\mathrm{CO}}_{\mathrm{a}}^{\mathrm{IASI}}\right)$ by 6$${\mathrm{CO}}_{\mathrm{adj}}^{\mathrm{GIIRS}}={\mathrm{CO}}_{\mathrm{ret}}^{\mathrm{GIIRS}}+\left({\mathbf{A}}^{\mathrm{GIIRS}}-I\right)\left({\mathrm{CO}}_{\mathrm{a}}^{\mathrm{GIIRS}}-{\mathrm{CO}}_{\mathrm{a}}^{\mathrm{IASI}}\right),$$ where ${\mathrm{CO}}_{\mathrm{adj}}^{\mathrm{GIIRS}}$ is the adjusted profile result; ${\mathrm{CO}}_{\mathrm{a}}^{\mathrm{GIIRS}}$ is the GIIRS a priori profile; ${\mathbf{A}}^{\mathrm{GIIRS}}$ is the GIIRS retrieval averaging kernel matrix. Figure 13 (third column) shows that this adjustment results in better agreements (smaller RMSE) between GIIRS and IASI. Furthermore, to test the impact of the small difference of $\mathbf{AK}$ (especially around 200 hPa) between GIIRS and IASI on the comparison, we applied the $\mathbf{AK}$ smoothing to the IASI-retrieved CO partial column profile retrievals (Sect. S1 in the Supplement). The results, as shown in Fig. S9, from IASI and GIIRS are highly consistent, suggesting the small difference in $\mathbf{AK}$ between IASI and GIIRS is not significantly affecting the comparison of CO columns.

For comparing the time series of GIIRS and IASI, we focus on the four representative regions (North China Plain, Mongolia, East China Sea and northern India) and compare the regionally averaged CO total columns between GIIRS and IASI. The data processing is similar to the spatial comparison. First, the retrieval data are re-gridded into 0.5${}^{\circ }$ $\times$ 0.5${}^{\circ }$ grids, and the comparisons are made using the collocated grid data points to avoid bias related to uneven distribution of CO data points within the selected region. Then, according to the averaged observation hour of IASI in a specific region, the temporally closest measurement cycle of GIIRS retrievals is used. Finally, the GIIRS CO retrievals are also adjusted to the IASI a priori following Eq. (6). The comparison results of daily averaged CO columns are shown in Fig. 14. The statistics of the comparisons are shown in Table S1 in the Supplement.

Figure 14

Comparison of daily CO total column between GIIRS and IASI averaged over (a) North China Plain, (b) Mongolia, (c) the East China Sea and (d) northern India. The retrievals are re-gridded to 0.5${}^{\circ }$ $\times$ 0.5${}^{\circ }$ grids in the selected region. The daily mean value for each region is computed when at least three grid points are available. The first column shows their time series in July 2022. The second and the third columns are the scatter plots for the daytime and nighttime daily averages. The adjusted data are generated by adjusting the GIIRS CO profile retrievals based on the IASI a priori CO profile.

[Figure omitted. See PDF]

The direct comparison between GIIRS and IASI shows good agreement, with the majority of the correlation coefficients larger than 0.8. Specifically, the daily variabilities are highly consistent between the two datasets. Since in their retrieval algorithms the a priori CO total columns used in GIIRS and IASI do not vary with days, the daily changes of the retrieved CO total columns directly reflect the available information in the observations from both instruments. This consistency between GIIRS and the state-of-the-art IASI CO retrievals demonstrates the effectiveness of FY-GeoAIR algorithm in constraining CO profiles from GIIRS. Note that in the nighttime, both instruments have weak sensitivity to the lower atmosphere; the agreement may just indicate that GIIRS and IASI have the same decreased sensitivity at nighttime. After correction using the a priori adjustment, we found that the changes are not uniform. While the consistencies for the nighttime cases improve for East China Sea and northern India, it becomes worse for Mongolia, probably due to the larger retrieval uncertainty under lower temperature conditions in the nighttime that cause an increase in spectral noise.

7 Discussions

7.1 Applicability of the FY-4B/GIIRS spectra for retrieving CO columns in the winter season

For IR sounders like GIIRS, observations of low-temperature targets are associated with high radiometric noise in brightness temperature, leading to unstable retrievals with large uncertainty. In the winter season when the surface and the atmospheric temperatures are dramatically reduced, the applicability of the GIIRS spectra in retrieving the CO columns is unknown. As a preliminary test, we apply the algorithm to observations in December when temperature is close to the lowest point. As shown in Fig. S10, the average temperatures in North China Plain and East China Sea drop by about 20 K, and in Mongolia the drop is more than 30 K. Although the TC can be large over these regions, the high spectral noise related to low temperature may significantly reduce the detectivity. As a result, the RMSE of the fitting residual averaged over all retrievals in December is $\mathrm{1.16}\pm \mathrm{0.82}$ K, which doubles the estimate ($\mathrm{0.63}\pm \mathrm{0.13}$ K) in July, as shown in Fig. S11. The DOFS for the majority of retrievals in the high-latitude regions has dropped to below 1.0, as shown in Fig. S12 with an example of CO column and DOFS maps at 03:00–04:00 BJT on 18 December 2022. If we apply the filter based on the RMSE of fitting residual $\le \mathrm{1.0}$ K, almost all the retrievals in the high latitude ($>\mathrm{40}$${}^{\circ }$ N) are filtered out. The availability of retrievals is much smaller for the nighttime observations due to its even lower temperature. Fortunately, since the sea surface temperature is relatively high in winter, the ocean regions in the low latitudes can still provide observations with low fitting residual and high DOFS that are comparable to summer retrievals.

7.2

Importance of a priori adjustment and$\mathbf{AK}$ smoothing for comparing retrievals

The importance of the $\mathbf{AK}$ matrix for intercomparison of retrievals has been described in detail by Rodgers and Connor (2003) using retrievals from MOPITT, an LEO IR sounder, as an example of a space-born instrument. Because of the highly variable TC over the diverse land cover in eastern Asia, the GIIRS retrievals present distinctive vertical sensitivity for different hours at different locations, which makes the interpretation of the retrieval results more difficult and, therefore, better use of the $\mathbf{AK}$ matrix more important. For comparison with model simulations, as illustrated in the simulated synthetic experiments in Sect. 5, a correction as in Eq. (5) is necessary given the model-simulated profile can be assumed to have uniform vertical sensitivity. For comparison with retrievals from other remote sounding instruments, which have different a priori and $\mathbf{AK}$ matrices, the a priori adjustment and $\mathbf{AK}$ smoothing correction as in by Rodgers and Connor (2003) are necessary to reconcile the retrievals. Because of the mismatch in observation footprints and the heterogeneity of the $\mathbf{AK}$ matrix over land, the collocation of sounding measurements from different instruments should also be carefully implemented to make sure the comparison is not biased due to inappropriate spatial interpolation.

8 Conclusions

Using hyperspectral infrared measurements from GIIRS on board FY-4B, we showed the first results of diurnal CO, an important trace gas in the atmosphere, measured from a GEO orbit. The performance of the algorithm is first evaluated by conducting retrieval experiments using simulated synthetic spectra. Retrieval results from 1 month of GIIRS spectra in July 2022 show that the DOFS for the majority is between 0.8 and 1.5 for the CO total column and between 0 and 0.8 for the bottom three-layer (from the surface to 3 km a.s.l.) atmosphere, which strongly depends on TC. Comparing the CO total column between GIIRS and IASI shows that the two datasets have good consistency in capturing the spatial and daily variabilities. This study demonstrates that the GIIRS retrievals are able to reproduce the temporal variability of CO total columns over eastern Asia in the daytime in July. Nevertheless, the retrievals have low detectivity in the nighttime due to their weak sensitivity to the ground level CO changes limited by low information content. Since CO plays an important role in tropospheric atmospheric chemistry and is an effective tracer of CO${}_{\mathrm{2}}$, the CO profile retrievals at a spatial resolution of 12 km and a temporal resolution of 2 h from GIIRS have great potential in improving local and global air quality and climate research through model assimilation that takes into account the associated vertical sensitivity. The operational geostationary observation by GIIRS represents an important advancement over the once-/twice-per-day observations provided by current LEO instruments.

In the coming future, CO observations from planning GEO missions, e.g., ESA's IRS and NASA's GeoCarb, along with GIIRS on board future FengYun satellite series, will greatly expand our capability in monitoring global CO emissions at high temporal resolution across Asia, Europe and America. Moreover, combining NIR and TIR to measure CO could further improve constraining the CO profile from GEO orbits, as the NIR adds information in the boundary layer while the TIR is more capable of distinguishing near-surface and mid-troposphere (Fu et al., 2016; Natraj et al., 2022), which will be another very important advancement in the future.

Appendix A  

Figure A1

(a) Bottom-up estimated CO emissions on 7 July 2022, from the CAMS model. These emissions include anthropogenic CO emissions from fossil fuel use on land, shipping, and aviation and natural CO emissions from vegetation, soil, the ocean, and termites. The emissions are in a unit of [kg m${}^{-\mathrm{2}}$ s${}^{-\mathrm{1}}$] at $\log \mathrm{10}$ scale. Four representative regions in black boxes are selected for inter-comparisons, including (1) North China Plain (covering 32–40${}^{\circ }$ N and 114–120${}^{\circ }$ E), which represents industrialized urban regions with persistently high CO emissions; (2) Mongolia (covering 42–50${}^{\circ }$ N and 100–115${}^{\circ }$ E), which represents CO background regions; (3) the East China Sea (covering 25–33${}^{\circ }$ N and 122–129${}^{\circ }$ E), which represents ocean surface; (4) northern India (23–28${}^{\circ }$ N and 75–83${}^{\circ }$ E), which represents urban CO source region in India. (b) Surface pressure from ECMWF ERA5 reanalysis for the surface layer on 7 July 2022; (c) The surface temperature from ECMWF ERA5 reanalysis for the surface layer on 7 July 2022.

[Figure omitted. See PDF]

Figure A2

Comparison of GIIRS and IASI DOFS for retrievals shown in Fig. 13. The DOFSs are re-gridded into $\mathrm{0.5}{}^{\circ }\times \mathrm{0.5}{}^{\circ }$ grids and the collocated grid data are compared for the daytime observation in panel (a) and nighttime in panel (b). A comparison of detectivity indicated by averaging kernel diagonals is shown in panels (c) and (d) from three selected locations, including observations in Mongolia in black, in North China Plain in red and in East China Sea in blue.

[Figure omitted. See PDF]

Data availability

The CO retrieval data from FY-4B/GIIRS are publicly available at 10.18170/DVN/M7DKKL (Zeng, 2022). Future updates on FY-4B/GIIRS CO data will be posted on https://opendata.pku.edu.cn/dataverse/FYGEOAIR (Peking University Open Research Data Platform, 2023); FY-4B/GIIRS Level 1 data are publicly available at http://satellite.nsmc.org.cn/portalsite/default.aspx (FengYun Satellite Data Center, 2023); IASI/Metop-B CO level 2 retrieval data are downloaded from https://iasi.aeris-data.fr/co/ (IASI AERIS database portal, 2023); IASI is a joint mission of EUMETSAT and the Centre National d'Etudes Spatiales (CNES, France). The authors acknowledge the AERIS data infrastructure for providing access to the IASI data in this study, ULB-LATMOS for the development of the retrieval algorithms, and EUMETSAT/AC SAF for CO/O3 data production. The surface emissivity datasets are downloaded from the Global Infrared Land Surface Emissivity: https://cimss.ssec.wisc.edu/iremis/ (UW-Madison Baseline Fit Emissivity Database, 2023). The ECMWF ERA5 reanalysis datasets are available at https://cds.climate.copernicus.eu/ (Copernicus Climate Data Store, 2023). The ECMWF atmospheric composition datasets are available at https://ads.atmosphere.copernicus.eu/ (Copernicus Atmosphere Data Store, 2023).

The supplement related to this article is available online at: https://doi.org/10.5194/amt-16-3059-2023-supplement.

Author contributions

ZCZ designed the study, developed the forward model and retrieval codes, carried out the experiments and result analysis, and prepared the manuscript. LL and CQ provided guidance on using the FY-4B/GIIRS L1 spectra data and carried out experiments for assessing spectra uncertainty. All authors reviewed the manuscript.

Competing interests

The contact author has declared that none of the authors has any competing interests.

Disclaimer

Publisher’s note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.

Acknowledgements

Zhao-Cheng Zeng acknowledges funding from the National Natural Science Foundation of China, National Key R&D Program of China and Fundamental Research Funds for the Central Universities at Peking University. The financial support by the High-performance Computing Platform of Peking University is also acknowledged.

Financial support

Zhao-Cheng Zeng has been supported by the National Natural Science Foundation of China (grant nos. 42275142 and 12292981), the National Key R&D Program of China (grant no. 2022YFA1003801) and the Fundamental Research Funds for the Central Universities at Peking University (grant no. 7101302981). This work has also been supported by High-performance Computing Platform of Peking University. Research at the National Satellite Meteorological Center (NSMC) was funded by NSMC of China Meteorological Administration (CMA) under the program of Calibration Technology Development and Level-1 Data Production for the Hyperspectral Imaging and Sounding Instruments on board FY-3E and FY-4B Satellites (grant no. FY-APP-2021.0507).

Review statement

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