Analysis of diurnal, seasonal and annual variations of fair weather atmospheric potential gradient at reduced number concentration of condensation nuclei from long-term measurements at Świder, Poland

Pawlak, Izabela; Odzimek, Anna; Kępski, Daniel; Tacza, Jose

doi:https://doi.org/10.5194/angeo-2024-1

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https://doi.org/10.5194/angeo-2024-1

Preprints

08 Mar 2024

| 08 Mar 2024

Status: this preprint is currently under review for the journal ANGEO.

Analysis of diurnal, seasonal and annual variations of fair weather atmospheric potential gradient at reduced number concentration of condensation nuclei from long-term measurements at Świder, Poland

Izabela Pawlak, Anna Odzimek, Daniel Kępski, and Jose Tacza

Abstract. The ground-level atmospheric potential gradient (PG) has been measured with a radioactive collector method in Stanisław Kalinowski Geophysical Observatory in Świder (52.12° N, 21.23° E), Poland, for several decades. Long-term measurements analysed previously revealed rather typical behaviour in the diurnal and seasonal variations of the PG of a land station controlled by pollution. Observation of the potential gradient at such a station usually show a maximum at local winter months which are mostly affected by anthropogenic pollution. The 1965–2005 series has been newly analysed to describe the Świder PG variations in greater detail, also in connection with an analysis of simultaneous measurements of condensation nuclei measured at 6, 12, 18 UT. An attempt is made to calculate the diurnal and seasonal variations at condensation nuclei number concentrations below 10000 cm^-3. There is a decrease of the PG in the diurnal variation by up to 11 % in the winter, and no significant change in the summer. The reduction in the annual variation is 11–26 % with the biggest difference in February. In the summer months, this difference is negligible. Such differences can be predicted with a simplified model of electrical conductivity including the aerosol composition of water soluble and soot particles, the main components of continental aerosol. With this model we obtained changes in the conductivity and the PG in up to 30 % in the winter, and 6 % in the summer. Despite the efforts to minimise the aerosol effect on the PG, the character of the PG seasonal and annual variation preserves its character with a maximum in the Northern Hemisphere winter and the minimum in the summer.

Received: 16 Feb 2024 – Discussion started: 08 Mar 2024

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Izabela Pawlak, Anna Odzimek, Daniel Kępski, and Jose Tacza

Status: final response (author comments only)

RC1:
'Comment on angeo-2024-1', Earle Williams, 03 Apr 2024

Publisher’s note: a supplement was added to this comment on 8 Apr 2024.
The authors should be encouraged to interact with Marek Kubicki of the same institution in Poland, and work to incorporate the conductivity data in this study.
Please see also longer review attached below.

Citation: https://doi.org/10.5194/angeo-2024-1-RC1
- AC1: 'Reply on RC1', Izabela Pawlak, 30 Jun 2024
  
  We thank both reviewers for the insightful and helpful comments and for the careful reading of the manuscript. For the revision we finished the digitisation of conductivity data published in Swider observatory yearbooks 1965-2005, and performed additional analyses recommended by Reviever #1 and Reviever #2, as well as researched some technical details of the instrumentation used for CN concentration measurements at Świder. Although Reviewer #1 recommended the use of air conductivity data as more appropriate for the search of annual GEC maximum we would like to explain that the aim of our original submission was, among others, to perform an analysis using PG and CN data to investigate the annual variation in the hope of reaching some conclusions in regard to GEC annual variability, and we do not claim our results solve the problem of the GEC maximum. Reviewer #2 regards the material as useful in the investigations of the relationship between the potential gradient and aerosol concentration, which was one of our aims, as well as analysis of diurnal and annual variations of these variables taking into account all values obtained during fair weather conditions. We wish to reconcile the differing advice of the Reviewers by adding an additional section that shows new results based on analysis of both the PG and conductivity that puts some more light on the GEC annual variation problem, or to clarify the purpose and conclusions of the analysis made more strongly.
  Below we respond to the comments made by Earle Williams, the Reviewer #1.
  The main goal of this study, the assessment of the seasonal variation of the global electrical circuit from a polluted continental location, is very worthwhile and strongly appreciated, and from that standpoint every effort should be made to get the work published. The true seasonal variation of the DC global circuit is still not firmly established, even in measurements of the ionospheric potential (with contradictory seasonal variations from Muhleisen/Fishcer and from Markson). My main concern, already communicated to the second author, is the limited approach taken here: the measurement of condensation nuclei to characterize the atmospheric medium, rather than the measurement of air conductivity with a pair of Gerdien tubes. In the following, suggestions are made for improving the present approach, but in the end we suggest a conductivity approach that rests on observations readily available to the authors at the same Swider location (by Marek Kubicki).
  
  Summary: Consider for publication after major revisions (and possible inclusion of conductivity measurements)
  Reply: We thank the Reviewer for the careful and critical reading of the manuscript and the constructive comments made. After completing the digitisation of all Świder atmospheric electric 1965-2005 data, we are also able to present new results that include analysis of the annual variation of the conductivity measured at Świder (by the Gerdien tube). More details and a new plot are given below and in the attachment to this response.
  Response to substantive issues:
  (1) Characterization of the medium with a CN counter
  For reasons of time, the authors have been reluctant to get involved with the Swider conductivity measurements, and instead have chosen to rely on a CN counter. (The distinction between large and small ions of atmospheric electricity is not mentioned.) If the large ion population is reliably measured with the CN counter, then the air conductivity can be inferred (though this is not the best approach to obtaining air conductivity, as it is an indirect one). Unfortunately, the documentation on what is being measured with the Scholz counter is thin, even to the point of not disclosing what supersaturation value is achieved. It would also be valuable to know the instrument response to clean oceanic air but that is of course not easily obtained. In any case, a big improvement in the characterization of the Scholz counter is essential here.
  Reply: In this study we wanted to concentrate rather on PG and aerosol number concentration as the PG is the most commonly observed atmospheric electric parameter worldwide, and there are more and more observations of aerosol concentrations, so other stations could make a similar analysis to investigate the results at their location.
  We admit the information about the instrumentation for aerosol concentration measurements is limited as it is very scarce in the observatory yearbooks. We would like to add more details about the measuring apparatus which we found in the literature, in the archive materials of the Institute and from the observatory staff. A Scholz counter is a type of condensation counter constructed by Scholz as an improvement of the Aitken counter (McMurry 2000), designed to measure the concentration of condensation and nuclei nearly the total concentration of aerosol. Supersaturation of >20% are required to measure the concentration of condensation nuclei (Deshler 2003). At Świder, the main part of the small Scholz counter was a brass cylindrical chamber with a volume of 102 cm3 and a height of 4 cm, with which the adiabatic expansion ratio of 1:1.25 could be achieved. The Scholz counter allows measurements in a wide range of CN concentrations from 5 to 960 000 particles in cm3. We have not found any information on the experimental error, however, it should not be higher than the experimental error of the Aitken counter which is about 10%. The Scholz counter was used by the end of 1982 and after which a photoelectric counter was used as a more convenient (automatic) replacement. It was based on the construction of a Verzár counter which had the condensation chamber of 680 cm3 in the volume.
  (2) The conductivity model used here
  Section 6 describes a conductivity model, but without sufficient details to thoroughly check its viability and origin. Equation (1) represents this model, but this is not an equation found in Tinsley and Zhou (2006). It may be an equation taken from Israel’s text, but that is not identified. I for one do not recognize equation (1) from available references, though the inverse relationship between conductivity and N is reasonable. In addition, all parameters used here should be properly quantified and justified. One piece of evidence that this conductivity model is not working properly (even if equation (1) is taken at face value) is a simple check on Ohm’s Law and air-earth current. One need only check equation (2) numerically (though it should be born in mind that the GEC air-earth current may vary annually). For winter, a value σ = 2.28 x 10^-15 and E = 370 V/m, J = 0.84 pA, too small by at least a factor of two. For summer, σ = 1.76 x 10^-15 and E = 370 V/m, J = 0.65 pA, and so too small by a factor greater than three. The evidence here is that the conductivity model is giving too small a conductivity, and that inference is backed up by the large values of N coming out of the CN counter (with values per cc larger than ones typically reported in the literature, even for cities, see Chalmers (1967). The authors should make these points and these calculations. They also need to take a careful look at their conductivity model.
  Reply: We apologise for giving the wrong reference to Eq. 1. Tinsley and Zhou (2006) in their Eq. 3 give a differential equation, the solution of which is our Eq. 1. This equation can also be found in Schonland (1932), Makino and Ogawa (1985), among others. The input parameters for the conductivity model are also taken from other published models of the air electrical conductivity (which use the same Eq. 1), such as Makino and Ogawa (1985), Sapkota and Varshneya (1990), Tinsley and Zhou (2006), Kulkarni (2022). Every parameter used is based on empirical models (e.g. ion production) or other experimental data. The ion mobility of 1.5 cm2 s-1 V-1 seems a realistic value for both positive and negative atmospheric ions at altitudes of up to 15 km according to Swider (1988). The ion recombination coefficient of 1.4 x 10-6 cm3 s-1 was used by Kulkarni (2022), similarly to Makino and Ogawa (1985). Ion production by cosmic rays of the order of 1.0 s-1cm-3 is appropriate for the production at the ground level, and of the order of 1.0 s-1cm-3 for the production by radioactivity from radon (8.6 s-1 cm-3 in Makino and Ogawa (1985) over land). In the correction we would like to update the ion production value to 2.5 s-1 cm-3 which gives more realistic values of the conductivity at Świder. We also need to correct ion recombination coefficient α since our calculations were made with α = 1.3 x 10-7 cm3 s-1. We leave the values of the beta coeficient of ion attachment rate calculated following the method of Tinsley and Zhou (2006) which uses the aerosol parameters of Hess et al. (1998). Hess et al. (1998) use constant model distributions of the aerosol constituents (soot, water soluble, insoluble and others) while in reality these distributions may also vary depending on seasons and day. In general, it is still a simple conductivity model which still needs to rely on several input parameters for various processes present such as the ion production, the rates of ion recombination and ion attachment to aerosol particles. For these parameters we use representative values used in other conductivity models while in reality these values may vary over a wider range, and in fact to have realistic model of local conductivity we need more observations to derive the required parameters.
  We want to further simplify the presentation of the model by calculating the results for resulting ion conductivity when the relative proportion of water soluble and soot components varies, and later we assign selected situations to winter and summer conditions (previously, the summer conductivity model was just a subset of the results for winter, only with smaller CN concentrations). We also calculate the effective βeff coefficient. The details are given in the attachment.
  
  (3) The arbitrary CN threshold of 10,000 per cc
  This threshold in CN is mentioned repeatedly (lines 8, 45, 99, 103, 111, in captions for Figures 7 and 8, lines 177, 341 and 347), but it is not made clear why this value was selected. No reference is given for justification. The suggestion is that the authors are seeking a characterization of the medium in cleaner conditions, but again the best parameter for that purpose is the Gerdien-measured conductivity, since this quantity is dominated by small ions with mobilities orders of magnitude larger than those for large ions/CN). In the end, the selection of this threshold is not resolving the main troublement at present (lines 13-14 of the Abstract and lines 360-362 of the Conclusions).
  Reply: We have given the reference in line 47 (Mohnen and Hidy 2010, after Landsberg 1938). Values of condensation nuclei number concentration of the order of several thousand particles per cc (i.e. below 10000 cm-3, and we considered levels of CNs <10000, <8000, <6000 and <4000 per cc, the latest being too rare for statistics). Schonland (1953, Table II) cites the results of CN measurements from Heligoland (6300 per cc) in the conditions of wind from the direction of land. Junge (1959) presents the results of Lansberg (1938) in a different way, with 9500 per cc being average CN concentration for an open country, and 5900 per cc a mean minimum concentration for a town – these are the conditions we aimed to investigate.
  (4) The main troublement of the paper
  The authors’ main troublement, linked directly to the important interest in the annual variation in the source of the global electrical circuit, is that the seasonal variation in N (and conductivity inferred from the model that is N-dependent) is quite small in comparison with the potential gradient, leaving the impression that NH winter is still dominating the DC global circuit, as Lord Kelvin had inferred (probably incorrectly) more than a century ago. Based on the weight of the evidence now available, something is wrong with using the CN measurements to infer the true air conductivity.
  Reply: Yes, the interest in the annual variation of the global electrical circuit was for us an important issue and one for the purpose of which we carried out the investigation, however, in the first place we wanted to investigate whether, having a long-term series of PG and CN measurements we would be able select the conditions of low aerosol concentration, and whether this could reveal a different character of the annual variation of the PG. It did not, however, since the PG still had a maximum over NH winter months, and we never said that corresponded to the annual maximum of the GEC. Perhaps we have not emphasised this conclusion of our paper enough. We agree that using only 3 hours from each day may not represent total seasonal or diurnal variation but it does represent some characteristic points that capture the variation of CN during a day (Fig. 6).
  
  (5) The suggested resolution of the troublement
  The good news here is that long-term Gerdien tube measurements of the air conductivity are also available at Swider and have been presented in earlier unrefereed work by Kubicki et al. (2007), in a work that is cited in the present manuscript (page 2) but not elaborated on in the present context. The air conductivity is always dominated by the small ions (whose mobilities are orders of magnitude larger because of their small size, but these are not the ions measured with typical CN counters). Figure 1b of Kubicki et al. shows that the wintertime conductivity of air is reduced by a factor of two in comparison with summer, and is inverse with the measured seasonal change in potential gradient, making the seasonal variation in air-earth current much less than either conductivity or PG. The most important point here is that the seasonal change in air conductivity is MUCH LARGER than the variation of CN, the main source of the authors’ troublement.
  
  One last aspect of Kubicki et al. (2016) that also has relevance is Figure 1a, showing that the seasonal variation of dust exceeds a factor of 5, and so shows the largest seasonal variation of all. It is conceivable that the dust (however it is measured, and this is not explained in this brief abstract) is dominating the removal of small ions over the seasonal cycle. One must also be aware however (from Figure 6 of the reviewed work) that the true seasonal variation of CN is not captured by the 3-hour per day sampling of CN, a serious shortcoming.
  Reply: The conductivity measurements have been carried at Świder, however the observatory yearbooks report only the value of the positive conductivity. By now we have digitised the whole 1956-2005 series and are able to present some analysis of the data. The annual variation of the conductivity confirms earlier results of Kubicki et al. with a minimum in NH winter months and twice higher values in the summer.
  
  Summary: When air conductivity measurements at Swider are considered, and the authors can surely do that in a revised submission, the main troublement of the manuscript is removed. (This finding would not conflict with the Kubicki et al findings because the seasonal issue was not focused on in that work.) The revised findings would then support the general conclusions of Adlerman and Williams (1996) that the wintertime maximum in potential gradient is caused by the enhanced pollution expected in wintertime at extratropical locations such as Poland and the UK of Lord Kelvin.
  Reply: Thank you for the detailed consideration given to our manuscript. We are willing to add more results including an analysis of the conductivity for the purpose of investigating its annual variation and conclusions for the GEC annual variation. Alternatively, we could conclude the work with a clear statement that considering the conditions of low condensation nuclei conditions does not change the character of the annual variation of the PG at Świder.
  Bibliography:
  
  Deshler, T., Observations in Chemistry (In situ)|Particles, Condensation particle counters, Encycl. Atmosph. Sci., 2003.
  
  Hess, M., Koepke, P., Schult, I., Optical Properties of Aerosols and Clouds: The Software Package OPAC, Bulletin of the American Meteorological Society, 79, 831 – 844, https://doi.org/10.1175/1520-0477(1998)0792.0.CO;2, 1998.
  
  Landsberg, H., Atmospheric condensation nuclei, Ergeb. Kosm. Phys., 48, 410, 1938.
  
  Makino, M., Ogawa, T., Quantitative estimation of global circuit, J. Geophys. Res., 90(D4), 5961 – 5966, https://doi.org/10.1029/JD090iD04p05961, 1985.
  
  McMurry P.H.: The History of Condensation Nucleus Counters, Aerosol Sci Tech., 33, 4, 297-322, https://doi.org/10.1080/02786820050121512, 2000.
  
  Mohnen, V., Hidy, G.M., Measurements of Atmospheric Nanoparticles (1875–1980). B. Am. Meteorol. Soc., 91. 1525-1540 doi:10.1175/2010bams2929.1, 2010.
  
  Sapkota, B., K., Varshneya, N., C., On the global atmospheric electrical circuit, J. Atmos. Sol. Terr. Phys., 22, 1, 1-20, https://doi.org/10.1016/0021-9169(90)90110-9, 1990.
  
  Schonland, B. F. J., Atmospheric Electricity, Methuen & Company Limited, London, 1932.
  
  Schonland, B. F. J., Atmospheric Electricity, Methuen & Company Limited, London, 1953.
  
  Swider, W., Ionic mobility, mean mass, and conductivity in the middle atmosphere from near ground level to 70 km, Radio Sci., 23, 3, https://doi.org/10.1029/RS023i003p00389, 1988.
  
  Tinsley, B. A., Zhou, L., Initial results of a global circuit model with variable stratospheric and tropospheric aerosols, J. Geophys. Res.-Atmos., 111, D16 205, https://doi.org/10.1029/2005JD006988, 2006.
  
  Citation: https://doi.org/10.5194/angeo-2024-1-AC1
RC2:
'Comment on angeo-2024-1', Anonymous Referee #2, 21 Apr 2024

The paper contains a reinterpretation of historic data to investigate the relationship between aerosol concentration and atmospheric potential gradient. Many investigations similar to this have used proxies or estimates for aerosol concentrations, so the inclusion of real aerosol data makes this a useful addition to the literature.
In my view, the manuscript could aid the reader more my adding more technical information on the measurements and some additional statistical analysis. The site description may be included in the references, but it would benefit the manuscript to put pertinent information on the measurement site and places of interest nearby. For example, how near is the measurement site to major population centers, roads, the coast or industry. This would aid in understanding potential sources of aerosol.
The measurement instrumentation is listed but more detail on the instruments used would also be helpful. Of particular importance is the measurement range, sensitivity and error of the aerosol measurement. I believe more detail of the aerosol instrumentation needs to be repeated within the manuscript, as the references are not easily available. Please could you include details of what kind of aerosol counter is used, the size range that are counted and details of inlet tubing. In section 2.3, who assessed the criteria for fair weather, was this done by observatory staff, or more recently?
Finally, I would suggest that the paper could be strengthened by adding some more statistical testing to the analysis. For example, it is claimed that limiting the condensation nuclei concentrations does not significantly change the distributions of corresponding potential gradient values – was a test used to prove the difference is not significant? When comparing the shape of distributions, could you consider using a non-parametric distribution test, eg, Kolmogorov-Smirnov test?
A few small corrections:
Section 2.1, there was a change if instrumentation, was any cross checking done to verify if there was a change in response?
In Figure 1, is there any exclusion criteria before a data point can be included, for example, is there a minimum number of fair weather data points required for the month to be included?
In Figure 2 (and some subsequent figures) the values separated by commas are not clear which plot they belong too and this should be made explicit.
In Figure 6 can you clarify how long the measurement is that the means at 6h, 12h and 18h are?
Line 47: in the statement ‘less than 10,000’ could you say what size these particle fall under?
Line 228: What is the justification for the values given for the variable in equation 1, are they based on measured quantities?
Line 230: What is the justification in assuming both mobilities are equal, as they are often not different to each other. Is it possible to run a sensitivity analysis to see what a difference would make?
Line 242: Please provide more information on where and when these size distributions were measured.
Line 254: Why was relative humidity excluded?
Some smaller changes:
Line 133, change “except of” to “except in”
Line 176, superscript should be -3
Line 273: Should this read 1.3 times by?

Citation: https://doi.org/10.5194/angeo-2024-1-RC2
- AC2: 'Reply on RC2', Izabela Pawlak, 30 Jun 2024
  
  We thank both reviewers for the insightful and helpful comments and for the careful reading of the manuscript. We wish to reconcile the differing advice of the Reviewers by adding an additional section that shows new results based on analysis of both the PG and conductivity that puts some more light on the GEC annual variation problem, or by clarifying the conclusions of the paper more strongly. Below we respond to the remarks of the Reviewer #2.
  Reviewer #2
  
  The paper contains a reinterpretation of historic data to investigate the relationship between aerosol concentration and atmospheric potential gradient. Many investigations similar to this have used proxies or estimates for aerosol concentrations, so the inclusion of real aerosol data makes this a useful addition to the literature.
  
  In my view, the manuscript could aid the reader more my adding more technical information on the measurements and some additional statistical analysis. The site description may be included in the references, but it would benefit the manuscript to put pertinent information on the measurement site and places of interest nearby. For example, how near is the measurement site to major population centers, roads, the coast or industry. This would aid in understanding potential sources of aerosol.
  Reply: Indeed, we could add additional information about the measurement site. The PAS Geophysical Observatory in Świder is located in the central part of Poland in the Warsaw suburban area, about 25 km south-east. Świder used to be a popular holiday and health resort village located on the Świder river. The distance to the nearest urban center, which is the district town of Otwock, is 2.5 km. There is no major industry in the area but there are local anthropogenic sources of air pollution from heating, very typical for these suburban conditions. The architecture is dominated by residential buildings and mainly includes single and multifamily houses. The Observatory is located is less populated area nearer the river and covers about 7 ha. It includes the main office and three observation pavillions, two residential buildings are in a distance. The entire area is surrounded by trees (predominantly pine trees), with several clearings. In one of these clearings of an area of approximately 1 ha, one pavilion and the station’s instruments for atmospheric electricity and meteorology observations are located.
  
  The measurement instrumentation is listed but more detail on the instruments used would also be helpful. Of particular importance is the measurement range, sensitivity and error of the aerosol measurement. I believe more detail of the aerosol instrumentation needs to be repeated within the manuscript, as the references are not easily available. Please could you include details of what kind of aerosol counter is used, the size range that are counted and details of inlet tubing.
  Reply: We admit the information on the details of the apparatus is scarce as it is also very scarce in the observatory yearbooks, especially in regard to the technical details of the counters. We would like to add more details about the measuring apparatus which we found in the literature, in the archive materials of the Institute and from the observatory staff. We also add some details of the methodology and schedule of observations.
  Measurements of concentration of condensation nuclei (CN) in Geophysical Observatory in Świder between 1965 and 2005 were carried out using two counters: a small Scholz counter and a photoelectric CN counter built in the observatory and using chamber of a Verzár counter as a base. The measurement method used in both counters was the process of condensation of water vapor on atmospheric aerosol particles present in the measurement chamber, followed by a quantitative analysis of the resulting mist droplets. We intend to add literature references where these counters are described in more detail, e.g. McMurry (2000). Observations were performed three times a day between 5:50 GMT and 6:20 GMT (till 1971), 6:10 GMT and 6:30 GMT (afterwards), then between 11:00 GMT and 11:30 GMT, and between 19:00 GMT and 19:30 GMT (till 1971), 18:10 UT – 18:30 UT afterwards. These three periods of observations are referred to in the yearbooks as 06, 12, and 18 GMT or UT, respectively.
  
  At Świder, the main part of the small Scholz counter was a brass cylindrical chamber with a volume of 102 cm3 and a height of 4 cm, and the adiabatic expansion ratio of 1:1.25 could be achieved. Measurements were performed within the clearing of the meteorological station using the suction method, an air sample with a volume of 1 cm3 was taken at a height of 1 m above the ground surface. Measurements with a Scholz counter should be repeated a few times, and one measurement takes several minutes. The Scholz counter allows measurements in a wide range of CN concentrations from 5 to 960 000 particles in cm3. We have not found any information on the experimental error, however, it should not be higher than the experimental error of the Aitken counter which is about 10%.
  
  Since January 1983, the measurements have been performed with the photoelectric CN counter that was placed inside a measurement pavilion. The air samples were collected from the outside of the building at a height of 1 m above the ground. The suction of air was made through a 1 m long rubber pipe using an electric rotational pump. According to the yearbooks the counter enabled measurement of the concentration of CN whose radius ranged from 0.005 to 10 µm. The measuring range of the counter was 4500 to 850 000 CN in 1 cm3 of the air. The basic measurement of the number of CN took place in a cylindrical chamber filled with the tested air sample of the volume equal to 680 cm3. Estimates of the number of droplets were obtained using a photoelectric counter system by measuring the extinction of light. The electronic circuit system was built (also patented) by Stanisław Warzecha. The measurement accuracy was 15%.
  
  In section 2.3, who assessed the criteria for fair weather, was this done by observatory staff, or more recently?
  The criteria for fair weather were assessed by the observatory staff on an ongoing basis. The information is also included in the yearbooks.
  Finally, I would suggest that the paper could be strengthened by adding some more statistical testing to the analysis. For example, it is claimed that limiting the condensation nuclei concentrations does not significantly change the distributions of corresponding potential gradient values – was a test used to prove the difference is not significant? When comparing the shape of distributions, could you consider using a non-parametric distribution test, eg, Kolmogorov-Smirnov test?
  Reply: Thank you for pointing this out. We have tried to support our conclusions by using a non-parametric Kolmogorov-Smirnov (KS) and U Mann-Whitney (MW) tests. They have been used to calculate the statistical significance of differences between the PG distributions considering the decreasing number of CN. In regard to the distributions shown in Fig. 2 and in Fig. 7, both KS and MW tests indicated statistically significant differences (at the significance level of 0.05) between the PG-CN all and PG-CN<10000 distributions for the whole year as well as in the spring, autumn and winter. In case of the variations shown in Fig. 11, the KS test indicated statistically significant differences between the PG populations for all CNs and CN<10000, in January and February only. The MW test indicated such in April and November as well. When comparing PG and CN all with PG and CN<8000 the results of both tests indicate the statistically significant difference also in December, similarly to PG and CN<6000.
  A few small corrections:
  
  Section 2.1, there was a change if instrumentation, was any cross checking done to verify if there was a change in response?
  Reply: We don’t know exactly if any cross-checking has been done. In the yearbooks there is no information about it.
  In Figure 1, is there any exclusion criteria before a data point can be included, for example, is there a minimum number of fair weather data points required for the month to be included?
  Reply: No criterion regarding the minimum number of points for the months has been applied. Our intention was to use all the possible hourly values obtained during fair weather conditions.
  In Figure 2 (and some subsequent figures) the values separated by commas are not clear which plot they belong too and this should be made explicit.
  
  Reply: The values in Figures 2 and 7 separated by commas can be corrected by adding more description inside the figure panel as well as in the figures captions.
  In Figure 6 can you clarify how long the measurement is that the means at 6h, 12h and 18h are?
  Reply: As we mentioned, a single measurement lasted several minutes (about 5 min), and for any observation usually several single measurements were carried out and the final result was the average value calculated from these several measurements.
  Line 47: in the statement ‘less than 10,000’ could you say what size these particle fall under?
  Reply: The above statement refers to the number of CN below 10000 cm-3, we can suggest that there are particles from the whole measuring range (from 0.005 µm to 10 µm).
  Line 228: What is the justification for the values given for the variable in equation 1, are they based on measured quantities?
  Reply: Our intention was to use representative values of the necessary parameters, several of which are required for even such a simple conductivity model. Parameters of such order are used by various conductivity models which use values based on observational data or empirical models. These are the models of Makino and Ogawa (JGR 1985), Sapkota and Varshneya (1990), Tinsley and Zhou (2006), or Kulkarni (2022). Ion production by cosmic rays of the order of 1.0 s-1cm-3 is appropriate for the production at the ground level, and of the order of 1.0 s-1cm-3 for the production by radioactivity of radon. In the correction we would like to update the ion production value to 2.5 s-1cm-3 which gives more realistic values of the conductivity. The ion mobility of 1.5 cm2 s-1 V-1 seems a realistic value for both positive and negative atmospheric ions at altitudes of up to 15 km according to Swider (1988). We give more details on the changes to the model made in our response to Referee #1.
  Line 230: What is the justification in assuming both mobilities are equal, as they are often not different to each other. Is it possible to run a sensitivity analysis to see what a difference would make?
  Reply: As mentioned above the same value of (1.5 +- 0.3) cm2 s-1 V-1 could be used for both positive and negative ions. A change of the mobility by 0.1 cm2 s-1 causes a change in the conductivity by about 5 x 10-17 S/m (5%) which is rather small in comparison with the effect of other parameters considered.
  Line 242: Please provide more information on where and when these size distributions were measured.
  The information is taken from Kubicki et al. (2016), and the distributions were measured at the Świder Observatory after 2010. The data have not been published, however.
  Line 254: Why was relative humidity excluded?
  Reply: The effect of humidity would complicate the conductivity model even more, and we are unable at the moment to use a practical conductivity model that takes it into account. The aerosol concentration distribution parameters of Hess et al. (1998) used for the calculation of the ion attachment rate are given for the relative humidity of 50%. We consider it is appropriate for average fair weather conditions, even though observational values may cover a wider range.
  Some smaller changes:
  
  Line 133, change “except of” to “except in”
  
  Line 176, superscript should be -3
  
  Line 273: Should this read 1.3 times by?
  Reply: Thank you for the detailed consideration given to our manuscript. We confirm these are mistakes which could be corrected.
  Bibliography:
  
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  Citation: https://doi.org/10.5194/angeo-2024-1-AC2

Izabela Pawlak, Anna Odzimek, Daniel Kępski, and Jose Tacza

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Month	HTML	PDF	XML	Total
Mar 2024	98	22	4	124
Apr 2024	178	13	12	203
May 2024	48	8	8	64
Jun 2024	7	4	2	13
Jul 2024	46	21	7	74
Aug 2024	28	4	3	35
Sep 2024	14	4	0	18
Oct 2024	11	3	0	14
Nov 2024	4	1	0	5

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Short summary

The electric state of the Earth’s atmosphere is manifested in the surface electric potential gradient (PG). In fair weather the PG should follow the variation of the global source of electric current in the atmosphere, called the global electric circuit. The PG is also influenced by local conditions. We use long-term series of PG and analyse PG variations during conditions of low aerosol concentrations to minimise the aerosol influence on PG obscuring its change due to the global source.


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