Open Access

Tropospheric ozone column retrieval from OMI data by means of neural networks: a validation exercise with ozone soundings over Europe

  • Antonio Di Noia1, 5Email author,
  • Pasquale Sellitto2,
  • Fabio Del Frate1,
  • Marco Cervino3,
  • Marco Iarlori4 and
  • Vincenzo Rizi4
EURASIP Journal on Advances in Signal Processing20132013:21

https://doi.org/10.1186/1687-6180-2013-21

Received: 15 July 2011

Accepted: 18 January 2013

Published: 19 February 2013

Abstract

The retrieval of the tropospheric ozone column from satellite data is very important for the characterization of tropospheric chemical and physical properties. However, the task of retrieving tropospheric ozone from space has to face with one fundamental difficulty: the contribution of the tropospheric ozone to the measured radiances is overwhelmed by a much stronger stratospheric signal, which has to be reliably filtered. The Tor Vergata University Earth Observation Laboratory has recently addressed this issue by developing a neural network (NN) algorithm for tropospheric ozone retrieval from NASA-Aura Ozone Monitoring Instrument (OMI) data. The performances of this algorithm were proven comparable to those of more consolidated algorithms, such as Tropospheric Ozone Residual and Optimal Estimation. In this article, the results of a validation of this algorithm with measurements performed at six European ozonesonde sites are shown and critically discussed. The results indicate that systematic errors, related to the tropopause pressure, are present in the current version of the algorithm, and that including the tropopause pressure in the NN input vector can compensate for these errors, enhancing the retrieval accuracy significantly.

Keywords

Neural networksRemote sensingSatelliteOzone

1 Introduction

Tropospheric ozone is a key player in a number of atmospheric processes that affect both climate and air quality. Its climatic impact is expressed by a radiative forcing of about 0.35 W/m2, as estimated by the intergovernmental panel on climate change (IPCC) fourth assessment report [1]. Such radiative forcing makes tropospheric ozone the fourth atmospheric greenhouse gas by importance, following water vapor, carbon dioxide and methane [1]. As for the air quality, tropospheric ozone has both a positive and a negative role; its positive role lies in the fact that it acts as a precursor of the idroxyl radical, which is able to remove several pollutants from the middle troposphere through oxidation reactions [2]; its negative role lies in its toxicity for both humans and crops when it reaches high concentrations near the Earth’s surface [3, 4].

Monitoring the concentration of tropospheric ozone from a satellite platform offers the advantage of a temporally and spatially continuous observation, allowing the identification of long-range transport processes [5, 6], and the generation of temporally extended records, which are useful for the investigation of long term trends [79].

In the last two decades, the advent of a new generation of satellite hyperspectral atmospheric sounders, which make simultaneous radiance measurements with high spectral resolution and sampling rate, covering the ultraviolet (UV), visible (VIS) and infrared (IR) spectral ranges, has greatly enhanced our capability to detect and quantify several tropospheric trace gases, including ozone [10].

Among the tropospheric gases that can be monitored from space, ozone is one of the most problematic ones. In fact, the contribution of tropospheric ozone to the measured radiance signal must be separated from the contribution of stratospheric ozone, which is much larger, due to the fact that most of the atmospheric ozone is found in the stratosphere. In order to accomplish this, several techniques were developed during the last 20 years. The rationale behind the first tropospheric ozone retrieval algorithms was to isolate the stratospheric ozone column by means of limb measurements [11, 12] or total ozone retrievals over high-altitude clouds [13, 14], and then subtract it from a co-located or neighboring measurement of the total ozone column. In the case of limb measurements, the separation between stratosphere and the troposphere is achieved thanks to the limb viewing geometry, whose line of sight does not encounter the atmospheric layers located beneath the upper troposphere/lower stratosphere (UTLS). In the case of measurements over high clouds, it is assumed that such clouds shield the underlying troposphere, and that the stratospheric ozone field does not have a significant horizontal variability within a certain number of neighboring pixels. If these assumptions hold true, it is possible to say that total ozone column retrievals over high altitude clouds actually represent stratospheric columns, which can be subtracted from total ozone columns retrieved over neighboring clear-sky pixels to yield an approximated value for the tropospheric ozone column. This type of approach has been mainly used over the Tropics, where high convective clouds are more frequent.

During the last decade, the improved sensitivity to the lower tropospheric layers that was achieved with new satellite instruments—including the Global Ozone Monitoring Experiment (GOME), the SCanning Imaging Absorption spectroMeter for Atmospheric CHartographY (SCIAMACHY) and the Ozone Monitoring Instrument (OMI)—has enabled the development of algorithms that directly derive tropospheric ozone information from ozone profiles retrieved through an optimal estimation (OE) scheme [1518].

OE retrieval schemes make use of forward radiative transfer models (RTMs), which are computationally intensive and require a consistent characterization of the whole atmospheric state, including the properties of clouds, aerosols and spectrally interfering trace gases (i.e., gases that have absorption features in the same spectral region as the trace gas of interest), which in most cases must be assumed a priori. This can cause the retrieval process to be slow and sensitive to wrong a priori assumptions, as well as to forward modeling errors [19].

An alternative approach to the direct determination of tropospheric ozone from satellite measurements is represented by neural network (NN) algorithms. Instead of explicitly using a forward model, NNs attempt to approximate the relationship between the measured radiance and the atmospheric parameter of interest directly by means of a nonlinear regression on a given training set [20]. In the case of atmospheric retrievals, the training set for a NN algorithm will consist of simultaneous realizations of the radiometric measurements and the geophysical process of interest. In addition, other parameters that can be useful to better constrain the relationship between the radiance measurements and the parameter to be retrieved (e.g., information on the observation geometry, other atmospheric parameters) can be given as inputs to a NN. For the training of a NN to be successful, a large and comprehensive training set must be built, possibly covering all the atmospheric situations that can be encountered in reality (e.g., heavy pollution events, tropopause folds).

Although the training process can be slow, a trained NN is able to operate very quickly, which is an attractive feature for operational retrievals. Furthermore, NNs allow to handle heterogeneous data in an easy way. This is an important feature when a complex model relating a large number of different quantities (e.g., atmospheric optical thickness, tropopause height and tropospheric ozone column) cannot be explicitly formulated, although it is known that a physical correlation between these quantities exists. On the other hand, a disadvantage of NNs lies in the difficult interpretation of their results. Such difficulty arises from the fact that the physical relationships underlying the retrieval process are represented by a NN in a purely numerical form, without any reference to the causal relationships that link the observed data. Because of this, NN retrieval schemes do not provide diagnostics that measure the relative contribution of each atmospheric layer to the retrievals and the number of independent pieces of information provided by the algorithm—such as the averaging kernels and the degrees of freedom for signal (DFS) [19]—whose computation requires an RTM.

NNs have been successfully applied in several branches of atmospheric remote sensing [21], including retrievals of ozone profiles [22, 23], total ozone [24] and tropospheric ozone column [2527]. Recently, a new NN algorithm for tropospheric ozone retrieval over the northern mid-latitudes from OMI data—named OMI tropospheric ozone column neural network (OMI-TOC NN)—has been proposed [26]. In the present article, the results of a validation of this latter algorithm with ozone soundings performed at a number of European stations are presented.

The article is organized as follows. In Section 2, a brief overview of the NASA Aura-OMI mission is given. In Section 3, a description of the OMI-TOC NN algorithm is given. In Section 4, the ozonesonde sites used for this validation and the co-location criteria are described. In Section 5, the validation results are shown, the temporal trends in the retrieval errors are discussed, and the importance of a parameter which was not originally used in the NN input vector—namely, the tropopause pressure—is demonstrated. The conclusions are drawn in Section 7.

2 The NASA-Aura mission and the OMI instrument

The NASA EOS Aura mission [28], started in 2004 with the launch of the homonymous satellite, aims at the study of the atmospheric composition, chemistry and dynamics. The scientific instrumentation onboard the Aura satellite includes the OMI instrument, as well as the tropospheric emission spectrometer (TES), the microwave limb sounder (MLS) and the HIgh resolution dynamics limb sounder (HIRDLS).

The OMI instrument [29] is a nadir UV/VIS imaging spectrometer, that measures direct and backscattered solar radiation in three channels; namely, the UV1 channel (270–310 nm), the UV2 channel (310–365 nm) and the VIS channel (365–500 nm). The UV1 and UV2 channels are the most important ones for ozone monitoring, because they cover the Hartley and Huggins absorption bands of the ozone molecule. The VIS channel is used for observations of clouds, aerosols and other atmospheric trace gases (e.g., nitrogen dioxide, formaldehyde). However, it does not cover the region of the ozone Chappuis absorption bands where the ozone absorption cross section is largest (i.e., about 530–610 nm), and thus it cannot be directly exploited in ozone retrievals.

OMI can observe the Earth’s atmosphere in three observation modes. In the main mode—called the Global measurement mode—OMI has a swath width of 2600 km, a nadir pixel size of 13×48 km2(along- × across-track) for the UV1 channel and 13×24 km2 for the UV2 and VIS channels. The pixel size increases in the swath direction for increasing distances from the satellite ground track. The OMI average spectral resolution is of about 0.4 nm in the UV1 and UV2 channels and about 0.6 nm in the VIS channel. The OMI Global measurement mode provides almost global coverage in one day. In principle, a complete daily global coverage is possible at midlatitudes. However, a complex instrumental effect, called row anomaly—which started to appear in the Level 1B data on June 25th of 2007—creates some gaps in the instrumental coverage. More informations on this effect are available from the Royal Dutch Meteorological Institute (Koninklijk Nederlands Meteorologisch Instituut (KNMI)) website [30].

In addition to the Global mode, two so-called “zoom-in” observation modes are available. In both modes the nadir pixel size is reduced to 13×12 km2. In the Spatial zoom-in mode the pixel size is reduced at the expense of the swath width, which decreases to 725 km; in the Spectral zoom-in mode the reduction comes at the expense of the wavelength range, which is limited to 306–432 nm [29]. Zoom-in observations are only performed during selected orbits.

3 The OMI-TOC NN algorithm

Recently, a NN algorithm for tropospheric ozone column retrieval from OMI reflectance measurements has been proposed [26]. From now on, this algorithm will be referred to as OMI-TOC NN. The design and optimization stages of the algorithm are thoroughly discussed in [26]. The OMI-TOC NN was trained and tested with an extended set of ozonesonde measurements taken at the northern midlatitudes between 2004 and 2008. The ozonesonde stations whose data were used in the training set are listed in Table 1. The OMI-TOC NN performances were found to be comparable, and in some cases slightly better, with respect to those of the trajectory enhanced tropospheric ozone residual (TTOR) [12] and OE [17] algorithms over a set of co-located ozonesonde measurements [26]. These results suggest that the OMI-TOC NN is a valuable alternative method for tropospheric ozone retrievals from OMI data.
Table 1

Summary of the stations used in the training set of the OMI-TOC NN. After[26]

Station

Country

Latitude

Longitude

N. co-locations

Barajas (Madrid)

Spain

40. 46°N

3. 65°W

107

Boulder

United States

40. 09°N

105. 25°W

95

Bratt’s Lake

Canada

50. 21°N

104. 71°W

108

Churchill

Canada

58. 75°N

94. 07°W

91

Egbert

Canada

44. 23°N

79. 78°W

103

Goose Bay

Canada

53. 30°N

60. 36°W

126

Hohenpeissenberg

Germany

47. 80°N

11. 02°E

360

Huntsville

United States

34. 72°N

86. 64°W

82

Isfahan

Iran

32. 48°N

51. 43°E

36

Kelowna

Canada

49. 93°N

119. 40°W

116

Legionowo

Poland

52. 40°N

20. 97°E

179

Lindenberg

Germany

52. 21°N

14. 12°E

161

Payerne

Switzerland

46. 69°N

6. 57°E

463

Sapporo

Japan

43. 06°N

141. 33°E

117

Tateno

Japan

36. 06°N

140. 10°E

120

Trinidad Head

United States

40. 80°N

124. 16°W

57

Uccle

Belgium

50. 80°N

4. 35°E

390

Wallops Island

United States

37. 89°N

75. 48°W

57

The input vector for the OMI-TOC NN consists of OMI spectral reflectances at 19 selected wavelengths, extracted from OMI Level 1b data; the solar zenith angle (SZA) and the total ozone column taken from the operational OMI Level 2 product. Only Global measurement mode data were used, because only this observation mode provides daily global coverage. The 19 wavelengths were selected according to an extended pruning (EP) technique [31]. This technique aims at reducing the dimensionality of an input vector for a NN by retaining only the most informative inputs, i.e., those who have the strongest influence on the NN output. Six of the selected wavelengths belong to the 305–307 nm range (covered by the OMI UV1 channel), while the remaining 13 wavelengths lie in the 322–325 nm range (covered by the OMI UV2 channel). The spectroscopic relevance of these two spectral ranges in the context of ozone retrievals is discussed in [27].

The dimensionality reduction of the reflectance spectra is useful for a number of reasons. First, using full spectra would lead to a very big input vector, which would in turn cause a need for a larger training dataset and longer training times. Second, there would be the risk of including irrelevant information in the input vector, which may compromise the learning capabilities of the NN (e.g., by causing overfitting).

In order to homogenize the spatial resolution of the input spectra, the UV2 reflectances were degraded to the spatial resolution of the OMI UV1 channel (see Section 2). The resolution degradation was performed through simple arithmetical averages between pairs of adjacent spatial pixels in the across-track direction.

The output quantity for the NN, i.e., the retrieved parameter, is the integrated ozone column between the surface and the 200 hPa pressure level. From now on, the name tropospheric ozone column (TOC) will be used when referring to this quantity. However, it must be pointed out that the choice of a static upper integration limit in the definition of the TOC—regardless of the actual tropopause height—might be rather inaccurate. The problems that can arise as a consequence of this choice are shown and critically discussed in Section 5.

4 Validation set and intercomparison methodology

Six European ozonesonde stations were used in the validation of the OMI-TOC NN: Ankara (Turkey), Izaña (Canary Islands, Spain), Lerwick (Shetland Islands, United Kingdom), Valentia Island (Republic of Ireland), L’Aquila and San Pietro Capofiume (Italy). No data from such stations were used during the training of the OMI-TOC NN. Data acquired between October 2004 and December 2008 were considered in this validation exercise. This is the same period that is covered by the training dataset of the OMI-TOC NN. This choice was made in order to ensure that eventual problems in the algorithm are not caused by instrumental changes that may have occurred after the period covered by the training set.

The data for Ankara, Lerwick and Valentia Observatory were taken from the World Ozone and Ultraviolet Data Center (WOUDC) archive. The data for Izaña were taken from the public archive of the network for the detection of atmospheric composition change (NDACC).

In addition to the data available from WOUDC and NDACC, data from two the two Italian ozonesonde stations of L’Aquila and San Pietro Capofiume were used.

The L’Aquila ozone soundings were performed by the University of L’Aquila and the Centre of Excellence for the integration of remote sensing techniques and modeling for the forecast of severe weather (Centro di Eccellenza di Telerilevamento e Modellistica numerica per la Previsione di eventi Severi (CETEMPS)). The ozonesonde station is located at the CETEMPS atmospheric observatory, Casale Calore di San Vittorino (42.3°N, 13.31°E, 683 m a.s.l.), near the town of L’Aquila. The ozonesondes are SPC-6A type electrochemical concentration cell (ECC) sondes [32, 33], interfaced with Vaisala RS-92 PTH (Pressure, Temperature, Humidity) radiosondes.

The ozone sounding activity at L’Aquila is performed within the framework of a collaboration between CETEMPS, L’Aquila University and the Italian Ministry for the Environment and Territory. The first soundings were performed in 1994. Since 2004, about two soundings per month have been regularly carried out on average. In the past, L’Aquila ozonesonde data were used in the validation of ozone profiles retrieved by the Michelson interferometer for passive atmospheric sounding (MIPAS), onboard Envisat [34, 35].

The San Pietro Capofiume ozone soundings were performed under the responsibility of the Italian National Research Council (Consiglio Nazionale delle Ricerche (CNR)) Institute for Atmospheric and Climate Sciences (Istituto di Scienze dell’Atmosfera e del Clima (ISAC)). The San Pietro Capofiume ozonesondes are ENSCI-Z type ECC sondes, interfaced with Vaisala RS-80 PTH radiosondes.

In the past, ozone soundings were regularly performed at San Pietro Capofiume from 1991 to 1995 [36, 37], and a specific campaign was organized in 1997 [37]. In 2004 and 2005, a sporadic sounding activity was carried out. However, it was subsequently interrupted due to scarcity of research funds. The data acquired during 2004 and 2005 were used in this study.

Within the above mentioned set of locations, different climatological characteristics are represented. This allows the geographical generalization capabilities of the OMI-TOC NN algorithm to be assessed, even at the upper and lower boundaries of the latitudinal range covered by the training set. Izaña is close to the African continent and not far from the Tropic of Cancer, and thus can be regarded as an hybrid midlatitude/subtropical station, being influenced by air masses coming from both the midlatitudes and the subtropics [38]. Lerwick and Valentia are characterized by an oceanic climate, and are subjected to advections of both midlatitude and polar air masses [39]. Hence, these stations can either behave as polar or midlatitude stations depending on the location of the polar front. Ankara, L’Aquila and San Pietro Capofiume can be regarded as typical midlatitude stations. Furthermore, all the stations are located in geographical areas that are not covered by the training set of the OMI-TOC NN algorithm. For this reason, validating the algorithm over this set of locations can give a reliable insight on its geographical generalization capabilities, as well as on its limitations.

In order to generate the validation set, the same co-location criteria as those used in the development of the OMI-TOC NN algorithm [26] were followed. Specifically, an ozone sounding and an OMI pixel were considered as co-located if two criteria were met: (i) the nominal coordinates of the ozonesonde station and those of the pixel center were no more than ±1°apart; and (ii) no more than 12 hours had elapsed between the ozone sounding and the Aura overpass on the ozonesonde station.

By using these criteria, a total of 808 input-output pairs for validation were created. The number of co-locations obtained for each station is given in Table 2. An exiguous number of co-locations was obtained for San Pietro Capofiume. However, such data have been included in the present study for sake of completeness.
Table 2

Summary of the stations used in the validation presented in this article

Station

Country

Latitude

Longitude

N. co-locations

Ankara

Turkey

39. 95°N

32. 85°E

112

Izaña

Spain

28. 29°N

16. 49°W

227

L’Aquila

Italy

42. 38°N

13. 31°E

76

Lerwick

United Kingdom

60. 13°N

1. 18°W

240

San Pietro Capofiume

Italy

44. 65°N

11. 62°E

12

Valentia Observatory

Republic of Ireland

51. 93°N

10. 25°W

141

5 Validation results

The validation results from October 2004 to December 2008 are shown in the scatter plot in Figure 1. The retrieved TOCs are given an the abscissa, the true TOCs are given as the ordinate. A root mean square error (RMSE) of 10.21 DU was found. This value is definitely larger than that found in the validation results shown in [26], over a different set of ozonesonde stations. Furthermore, from a visual inspection of the scatter plot, it is evident that the algorithm has a systematic tendency to underestimate tropospheric ozone values larger than about 60 DU and overestimate values smaller than about 25 DU. Some quantitative statistics confirm this impression: 29 out of 33 TOCs larger than 25 DU are overestimated, and 42 out of 48 TOCs larger than 60 DU are underestimated. In order to assess whether this behavior displays a geographical dependence, the validation results were separately analyzed for each station.
Figure 1

Scatter plot of true versus retrieved TOCs for all the stations considered in this study.

The scatter plots of true versus retrieved TOCs for each ozonesonde station are shown in Figure 2. It can be noticed that, whilst the Ankara and L’Aquila scatterplots have a fairly symmetrical shape, the scatter plots for Izaña, Lerwick and Valentia Observatory exhibit a quite pronounced underestimation tendency throughout the whole dynamical range of the TOC values.
Figure 2

Scatter plots of true versus retrieved TOCs divided by ozonesonde station.

One possible reason for the systematic underestimation of TOCs higher than 60 DU lies in the choice of 200 hPa as a static upper integration limit for the retrieved ozone column. In fact, if this TOC definition is used, extreme TOC values can be expected when the actual tropopause pressure exceeds 200 hPa (i.e., when the actual tropopause height is lower than the upper integration limit used in the OMI-TOC NN), because a large portion of stratospheric air—which is very rich in ozone—is included in the column over which the ozone profile is integrated in order to derive TOC. As a result, including the tropopause pressure in the input vector can help the NN discriminate such cases of enhanced TOC, and hence improve the overall retrieval accuracy.

In order to check the correctness of this hypothesis, an analysis of the retrieval error versus the actual tropopause pressure was carried out for each station. The tropopause pressure data were taken from the NCEP/NCAR Reanalysis 1 [40]. Plots representing the retrieval error against the tropopause pressure for each station are shown in Figure 3. A trend line, resulting from a quadratic fit of the retrieval error versus the tropopause pressure, is superimposed on each plot. It can be seen that the error trend is particularly clear on Lerwick and Valentia Observatory, where cases of tropopause pressures considerably greater than 200 hPa are most frequent.
Figure 3

TOC retrieval error versus tropopause pressure for all the ozonesonde stations considered in this study.

6 Correction of tropopause related errors

The results shown in Section 5 confirm the hypothesis that a relationship between the retrieval accuracy of the OMI-TOC NN and the tropopause pressure exists. Furthermore, they suggest that the use of tropopause information as an input for the algorithm has the potential to enhance the retrieval accuracy. For this reason, a first attempt was made to design a new NN algorithm receiving such information as an input. The OMI Level 1B data were co-located with the NCEP/NCAR tropopause pressure fields in order to generate training, testing and validation sets for the new NN. The same stations used in the OMI-TOC NN were used to train the new NN. A comparison between the two NNs in terms of training, test and validation RMSE is shown in Table 3. The standard deviations of the sonde TCOs in the three sets are also reported. It can be observed that the new NN has a lower RMSE with respect to the previous one on all the three sets.
Table 3

RMSE on training, test and validation sets for the OMI-TOC NN and its modified version

Dataset

TOC Std. [DU]

RMSE [DU]

  

OMI-TOC NN

Mod. OMI-TOC NN

Training

11.49

7.43

6.22

Test

11.23

8.03

7.20

Validation

11.83

10.21

8.40

The overall results for the set of ozonesonde stations considered in this article are shown in Figure 4. A significant reduction in the both RMSE and the bias is evident. Particularly significant is the reduction in the underestimation tendency for high values of TCO. Out of the 48 TCOs larger than 60 DU, 25 were found to be underestimated by the modified OMI-TOC NN, in contrast with the 42 underestimations found for the original NN (Section 5). In more formal terms, if TOCretr is the retrieved TOC and TOCsondeis the TOC measured by an ozonesonde, we can say that the conditional probability Prob(TOCretr<60 DU|TOCsonde≥60 DU) on the validation dataset can be estimated in about 88% for the original OMI-TOC NN described in [26] and about 52% for the modified NN proposed in this article.
Figure 4

Scatter plot of true versus retrieved TOCs for all the stations considered in this study, for the modified version of the OMI-TOC NN.

Table 4 summarizes the performances of both the OMI-TOC NN and its modified version in terms of RMSE and mean bias. Mean and standard deviation of the TOCs measured by the ozonesondes are also reported, in order to facilitate the interpretation of the validation results. The results divided by station are also shown, in form of scatter plots, in Figure 5.
Figure 5

Scatter plots of true versus retrieved TOCs divided by ozonesonde station, for the modified version of the OMI-TOC NN.

Table 4

Error statistics for the OMI-TOC NN and its modified version for all the ozonesonde stations considered in this article

 

Station statistics

OMI-TOC NN

Modified OMI-TOC NN

Station

N. data

Mean TOC

Std. dev.

RMSE

Mean bias

RMSE

Mean bias

  

[DU]

[DU]

[DU]

[DU]

[DU]

[DU]

Ankara

112

38.04

11.54

8.33

−0. 21

7.68

0.40

Izaña

227

37.38

8.31

8.67

−5. 46

8.71

−5. 97

L’Aquila

76

36.00

11.59

8.68

2.50

7.35

1.42

Lerwick

240

44.80

13.41

12.96

−9. 28

8.60

−3. 46

San Pietro

12

34.82

6.55

5.51

0.35

3.91

1.17

Capofiume

       

Valentia

141

43.31

11.54

9.63

−6. 18

8.88

−5. 54

Observatory

       

Overall

808

40.54

11.83

10.21

−5. 17

8.40

−3. 47

The improvements are evident on Ankara and L’Aquila, and dramatic on Lerwick and Valentia Observatory. Such improvements were not found on Izaña, which still appears to be the most problematic station amongst those shown in this article. From a visual inspection of the upper right panel of Figure 3, it is evident that the tropopause pressures over Izaña were most often far below 150 hPa (i.e., the tropopause was considerably higher than the corresponding altitude level) with regard to the ozone soundings used in this validation exercise. This suggests that Izaña mostly behaved as a tropical station, and thus portends poor performances of the OMI-TOC NN with air masses of tropical origin. This behavior appears reasonable, because the OMI-TOC NN was trained using only midlatitude data. Anyway, further investigations are ongoing in order to interpret this result.

In Figures 6 and 7, time series of true and retrieved TOC over the six stations considered in this article are shown for the modified OMI-TOC NN. Apart from the above mentioned case of Izaña, where a strong negative bias of the NN versus the ozonesonde data exists, a slight underestimation tendency can be observed over all the six stations considered in this article. Such tendency appears to be strongest during the summer months, as evident from the results on Ankara (Figure 6, above panel) and L’Aquila (Figure 6, below panel). Specifically, it appears that the OMI-TOC NN is not able to reproduce situations of enhanced TOCs that occur during the summer. It is still not clear whether this fact is caused by a lack of sensitivity of the algorithm to the lowest atmospheric layers. Appropriate actions, aimed at reducing this effect, should be taken in the development of further versions of the OMI-TOC NN algorithm.
Figure 6

Time series of true and retrieved TOCs for Ankara, Izaña and L’Aquila, for the modified version of the OMI-TOC NN.

Figure 7

Time series of true and retrieved TOCs for Lerwick, San Pietro Capofiume and Valentia Observatory, for the modified version of the OMI-TOC NN.

7 Conclusions

In this article, the results of a validation of a NN algorithm for tropospheric ozone column retrieval from OMI data—named the OMI-TOC NN—are shown. The validation was performed over six ozonesonde stations distributed across the European continent. This validation set is considered as a benchmark for the retrieval performances of the algorithm, as it represents a number of climatological situations that can be encountered over Europe.

A good agreement over Ankara, L’Aquila and San Pietro Capofiume—the most central stations in terms of latitude—was found. However, strong negative biases are present over Lerwick, Valentia Observatory and Izaña, especially in conditions of high TOC values. In order to investigate the reasons for this problem, the retrieval bias of the OMI-TOC NN algorithm was analyzed as a function of the tropopause pressure values taken from the NCEP/NCAR Reanalysis 1. A significant correlation between tropopause pressure and retrieval error was found. As a consequence, a new version of the OMI-TOC NN, having the NCEP/NCAR tropopause pressures in its input vector, was designed, and its results were evaluated over the same validation set.

The modified OMI-TOC NN algorithm exhibited a considerably improved retrieval accuracy, in terms of RMSE, over the whole validation set. The improvements were found to be most significative on the northernmost stations of Lerwick and Valentia Observatory, where cases of low tropopauses (i.e., high tropopause pressures) are most frequent. However, no improvements were observed on Izaña, where tropopause pressures larger than 200 hPa are quite unlikely. The results of the modified OMI-TOC NN on Izaña also suggest that using the tropopause pressure as an input for the algorithm is still not sufficient to improve the retrieval accuracy in cases of high tropopauses. In the future, this issue will be addressed by including tropical ozonesonde stations in the training set.

A major point that might be raised on the basis of these results is that using 200 hPa as upper integration limit in the TOC definition is not a sensible choice in order to characterize the tropospheric ozone column. Further versions of the OMI-TOC NN algorithm should provide estimates of the ozone column up to the actual tropopause, whether it be defined based on the NCEP/NCAR Reanalysis or by other means (e.g., dynamical tropopause).

Declarations

Acknowledgements

This study had been carried out in the framework of the ESA Project C1P.2930. All the PIs of the ozonesonde stations whose data are used in this study are gratefully acknowledged. The ozone monitoring activities of CETEMPS are partly funded by the Italian Ministero dell’Ambiente e della Tutela del Territorio e del Mare. The data for Ankara, Lerwick and Valentia Observatory ozonesonde stations were retrieved from the World Ultraviolet Data Center (WOUDC) archive (http://www.woudc.org). The data for the Izaña ozonesonde station were obtained as part of the Network for the Detection of Atmospheric Composition Change (NDACC) and are publicly available (see http://www.ndacc.org). The NCEP Reanalysis data are provided by the NOAA/OAR/ESRL PSD, Boulder, Colorado, USA, from their Web site at http://www.esrl.noaa.gov/psd/.

Authors’ Affiliations

(1)
Earth Observation Laboratory, Department of Civil and Computer Engineering, Tor Vergata University
(2)
Laboratoire Inter-universitaire des Systèmes Atmosphériques, UMR7583, CNRS—Universités Paris-Est et Paris Diderot
(3)
Istituto di Scienze dell’Atmosfera e del Clima, Consiglio Nazionale delle Ricerche
(4)
CETEMPS, Department of Physics, University of L’Aquila
(5)
SRON Netherlands Institute for Space Research

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