the Creative Commons Attribution 4.0 License.
the Creative Commons Attribution 4.0 License.
| 16 May 2025
Diel Variability Affects the Inorganic Marine Carbon System in the Sea-Surface Microlayer of a Mediterranean coastal area (Šibenik, Croatia)
Abstract. The ocean plays a crucial role in the global carbon cycle by absorbing and storing substantial amounts of atmospheric carbon dioxide (CO2). It is estimated that the ocean has sequestered approximately 26 % of CO2 emissions over the last decade, resulting in significant changes in the marine carbon system and impacting the marine environment. The sea-surface microlayer (SML) plays a crucial role in these processes, facilitating the transfer of materials and energy between the ocean and the atmosphere. However, most studies on the carbon cycle in the SML have primarily addressed daily variability and overlooked nocturnal processes, which may lead to inaccurate global carbon estimates. We analysed temperature, salinity, pHT25, and pCO2 using data collected over three complete diel cycles during an oceanographic campaign along the Croatian coast near Šibenik in the Middle Adriatic. Our analysis revealed statistically significant differences (p < 0.05) between daytime and nighttime measurements of temperature, salinity, and pHT25. These differences may be related to the occurrence of buoyancy fluxes, which are typically more pronounced during the day and could enhance CO2 fluxes, as observed with values of 1.98 ± 2.52 mmol cm−2 h−1 during the day, while at night, they dropped to 0.01 ± 0.02 mmol cm−2 h−1. These findings emphasise the importance of considering complete diurnal cycles to accurately capture the variability in thermohaline features and carbon exchange processes, thereby improving our understanding of the role of the ocean in climate change.
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Status: final response (author comments only)
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RC1: 'Comment on egusphere-2025-2090', Anonymous Referee #1, 08 Jul 2025
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AC2: 'Reply on RC1', Ander López, 19 Sep 2025
Comment
Response
The introduction primarily focuses on carbonate chemistry and the relevance of pCO₂ measurements, without adequately introducing the unique characteristics of the SML and its relevance to air–sea CO₂ fluxes (e.g., see the review by Cunliffe et al., 2013: https://doi.org/10.1016/j.pocean.2012.08.004). A more comprehensive and updated bibliographic foundation is needed. For example, in line 40, Cantoni et al. (2012) do not present trends in acidification but rather biogeochemical drivers of pH variability. Doney’s work is a milestone, but more recent references are necessary. Similarly, in line 52, Cantoni et al. (2016) do not mention the SML.
We thank the reviewer for all the valuable suggestions. We have revised the Introduction to highlight better the unique characteristics of the sea-surface microlayer (SML) and its role in air–sea CO₂ fluxes. In particular, we have incorporated the review by Cunliffe et al. (2013) as well as more studies (Engel et al., 2017; Mustaffa et al., 2020; Wurl et al., 2017), which emphasize the biogeochemical complexity of the SML. We also updated the references on ocean acidification, replacing Cantoni et al. (2012) with more appropriate and widely cited works (Orr et al., 2005; IPCC, 2021), and clarified the scope of Cantoni et al. (2016), which does not explicitly address the SML. In addition, we included Yates et al. (2007) to support diel variability of carbonate system parameters, and Kapsenberg et al. (2017) to reflect more recent regional trends in Mediterranean acidification. These changes provide a more comprehensive and updated bibliographic framework for our study.
The methods section is unclear. It lacks essential information needed to understand what was done, where, and on how many samples the study is based. The system used for data acquisition is not described, and there is no introduction to the study site or description of where the data were collected. See detailed comments in the manuscript.
We have added information to the Methods section to address the previous lack of detail, including a description of the study site, deployment strategy, variables measured, and considerations of measurement and calculation uncertainty, as well as environmental conditions. Specific changes requested by the reviewer are addressed in more detail in the responses to the following comments.
Line 63 – please add more references
We have included additional relevant references supporting the role of nocturnal respiration in driving increases in pCO₂ and decreases in pH.
Regarding carbonate system parameters, pH was measured continuously, but no details are provided about the electrode, calibration procedures, or accuracy. DIC and TA were measured using state-of-the-art methods on a limited number of discrete samples, as reported in Table 1: 3–4 samples during the day and 1–2 at night. These data were then used to calculate pCO₂ and pH at 25 °C. An estimate of the uncertainty associated with these calculations is necessary before discussing the results.
We note that:
- pH was measured continuously using the integrated sensor of the S3 flow-through system, reported on the total scale with a precision of ±0.005 pH units (Ribas-Ribas et al., 2017) and normalized to 25.43 °C to account for temperature variations, as already modified in the Methods section (Lines 148-149).
- Discrete DIC and TA samples were analysed with state-of-the-art methods (coulometric titration for DIC, potentiometric titration for TA), calibrated against certified reference material, with a 1σ measurement precision of ±3 µmol kg⁻¹ for DIC and ±2 µmol kg⁻¹ for TA. These values were then used to calculate pCO₂ with the CO2SYS program, and the associated uncertainties are inherent to these calculations.
We would like to clarify that pH was not calculated from DIC and TA; therefore, the uncertainty of DIC/TA does not apply. The precision and scale of the pH sensor, together with the temperature normalization, provide a reliable basis for evaluating diel and vertical differences.
Line 89 – Water depth? Distance from shore?
We have added details on water depth and distance from shore in the Methods section. Sampling was conducted in the lower estuary of the Krka River, immediately offshore from the St. Anthony Channel near Šibenik, with depths ranging from less than 2 m at the head of the estuary to about 42 m at the mouth (Cukrov, 2024; Prohic, 1989). The S3 catamaran operated along short transects within this representative area, allowing for the accurate characterization of the SML and the underlying water while minimizing spatial variability. These details are now included in the revised Methods section (lines 91–95).
Line 90 – on total scale? NBS scale? Accuracy? These data are the backbone for carbonate chemistry characterization some details are needed
In the revised manuscript, we now clarify that pH was measured using the integrated sensor of the S3 flow-through system, embedded in a custom-built flow cell following the original S3 design (see Ribas-Ribas et al., 2017), and is reported on the total scale. We also specify the sensor precision (±0.005 pH units), which is now explicitly mentioned in the text (lines 135-140) and detailed in Table 1.
Line 94 - please check and rephrase, "this study" is not the correct subject
We have changed the text accordingly.
Line 96 - How does the S3 system collect water? Is it a close system or open, in contact with atmosphere? There was somebody on board?
We have now expanded the description of the S3 system (Ribas-Ribas et al., 2017) to provide a more precise explanation of how SML and ULW waters are collected. The text specifies that water is collected via rotating glass discs and transferred into a closed flow-through system, minimizing atmospheric contact. We also clarified that the S3 was a remotely operated catamaran with no personnel on board and that discrete DIC and TA samples were collected separately from its outlets by approaching the catamaran with the support Zodiac. (lines 103-105).
Line 98- Every 30 seconds you collected a seawater sample, for 30-45 min (2x30 samples?)? Or this is for instruments? Please expline better
We did not collect discrete seawater samples every 30 seconds. Instead, the S3 system continuously pumped SML and ULW water through a flow-through system, and the sensors recorded temperature, conductivity, and pH at 30-second intervals during each 30–45-minute deployment. Discrete samples were not collected at 30-second intervals. Instead, DIC and TA samples were taken separately in small bottles directly from the S3 outlets by approaching the catamaran with a support zodiac and immediately sealed to minimize atmospheric contamination. This clarification has been added in the revised text (lines 115–117).
Line 99 - please find another way to define this, "noticeable" is not a scientific definition.
We have changed the text accordingly.
Line 134 - Use data from the ICOS station at Lampedusa or other interpolated pCO2 product, Mauna Loa is in a tropical area, it is not possible to use these data for atmospheric xCO2 in the Mediterranean area.
In the revised manuscript, atmospheric pCO₂ data are now obtained from the ICOS atmospheric station at Lampedusa (8 m height), which provides quality-controlled dry-air CO₂ mole fraction measurements representative of Mediterranean conditions (di Sarra et al., 2025). Specifically, we used the monthly mean for August 2020, corresponding to our sampling period. This ensures that the ΔpCO₂ values used in the flux calculations are regionally appropriate. The Methods section (Lines 160–166) has been updated accordingly, and the results have been recalculated; however, the revised results are very similar to the previous ones.
Line 135-137 - please explain better, it is not clear.
In the revised Methods, we now provide a detailed explanation of how the percentage error was determined. Specifically, we clarify that we computed mean fluxes for each diel cycle, including all available data (day and night), and compared them with mean fluxes derived from daytime measurements only. The relative difference was expressed as . We also note that both means were simple arithmetic averages of the available deployments. This revision (Lines 166–170) clarifies the procedure and explicitly highlights the rationale for quantifying the bias introduced by excluding nocturnal fluxes.
Line 148 - divide salinity-density correction and discussion from the carbonate chemistry section and move it above.
To improve clarity, we have introduced a new subsection heading for the salinity-density correction.
Line 195 (Figure 3) - check the units of salinity; Please explain better, how long are these timesteps?
The salinity units in Figure 3 are expressed in grams per kilogram (g kg⁻¹), consistent with the values reported in the Results. We have also clarified in the figure caption that each timestep corresponds to a 30–45 minute deployment (with data collected at 30-second intervals), with four daytime and two nighttime deployments per cycle.
Line 215 (Figure 4) - of the anomaly of temperature...
We have changed the text accordingly.
Line 286 - please add an explanation on how the temperature change affect the change in pHT25.
We have clarified in the Discussion that, although pH values were normalized to 25 °C to ensure comparability, the carbonate system speciation and CO₂ solubility remain intrinsically temperature-dependent. Thus, short-term cooling of the SML still leads to detectable changes in pHT25
The data discussion is weak. Various hypotheses are proposed to explain the observed variability, but these are not supported by further analysis or robust conclusions. For instance, in line 285 and following, the effect of evaporation on SML cooling is introduced, but the conclusion simply states that this affects pHₜ₂₅, without explaining whether it increases or decreases, and by which mechanisms. Other processes are mentioned without clarification. The overall conclusion is that "it is complicated, with an interplay of several factors," but this does not advance the current understanding.
In the revised Discussion (lines 327–330), we expanded the explanation of how physical processes affect pHT25. We now specify that carbonate speciation itself is temperature-dependent (Zeebe & Wolf-Gladrow, 2001), so short-term thermal fluctuations directly influence pHT25, even after normalization. In addition, we clarify that while evaporation tends to increase salinity and alkalinity, and thus pHT25, vertical mixing can counteract this effect by introducing water with lower pHT25 and higher pCO₂. These revisions replace the previous vague statement of “an interplay of several factors” with a mechanistic interpretation that links temperature, evaporation, and mixing to carbonate system variability, thereby strengthening the conclusions.
One of the main conclusions is the importance of including nighttime in the study of air–sea CO₂ fluxes. Wind speed and ΔpCO₂ are the primary variables controlling these fluxes, with wind dependence incorporated into the parameterization of “k” (line 131; Wanninkhof, 2014). Wind speeds were lower during the night (line 174), which would be expected to result in lower fluxes. However, the authors do not consider this aspect, and the relevance of diel ΔpCO₂ variability is not adequately discussed.
We agree that wind speed, via its effect on the gas transfer velocity (k), is the dominant factor controlling the magnitude of the fluxes in our dataset, consistent with the Wanninkhof (2014) parameterisation. This explains the clear contrast observed between daytime fluxes, when wind speeds increased, and nighttime fluxes, when calm conditions reduced the exchange to near zero. In our results, the diel variability of pCO₂ was not statistically significant (Table S2), suggesting that its role was secondary compared to wind forcing. Nevertheless, our observations also indicate that buoyancy fluxes linked to evaporation and density instabilities may have modulated daytime exchange, amplifying the effect of wind. In the revised Discussion,we have clarified these points: (i) wind is the primary driver of the diel variability in fluxes, and (ii) the inclusion of nighttime data is essential to avoid overestimation of daily means, since omitting the nocturnal period led to differences of 33–50% in our cycles.
Line 298-299 - You have already discussed the relevance of this process a few lines above, so you should elaborate more on the causes of the observed trends.
In the revised discussion, we have expanded our explanation of negative diurnal anomalies. We now clarify that, under the conditions of strong stratification and weak winds observed during the study, localized evaporative cooling and convection could have offset the expected surface warming, as described in previous studies on surface layer instabilities (Cronin and Sprintall, 2001; Soloviev and Lukas, 2014).
Line 303 - all this processes would change the salinity both in the SML and ULM and cannot be used to explain the anomalies.
We agree that external processes such as evaporation, river discharge, precipitation, or tides cannot explain the negative salinity anomalies between SML and ULW. In the revised Discussion (lines 338–344), we clarify that while evaporation tends to increase salinity, the consistently negative anomalies observed indicate that vertical mixing processes dominate over evaporation. External inputs (river, precipitation, groundwater, and tides) were negligible during the study period and would, in any case, affect both layers simultaneously. Therefore, we attribute the anomalies specifically to localized near-surface mixing.
Line 314 – 319 - the discussion is very weak, you should say more than just "is complex and there are several factors". e.g.: normalize pCO2 at a constant temperature and discuss the effect of biology on this parameter.
In the revised Discussion (lines 372–377), we strengthened the interpretation of Cycle 3. We now emphasize that the observed daytime increase in pCO₂ and pHT25 is best explained by biological and physical processes, rather than leaving it as a generic statement. Specifically, we discuss the likely contributions of enhanced respiration and CO₂ accumulation due to limited mixing, together with potential photoinhibition under high irradiance (Platt et al., 1980), which would reduce photosynthetic uptake. These additions provide a more precise mechanistic explanation for the observed pattern.
Line 331 – 334 - the main driver of this difference is wind, this has to be taken into account in the discussion.
We agree with the reviewer. The Discussion has been revised to state that wind is clearly the primary driver of the observed diel differences in CO₂ fluxes, in line with Wanninkhof's (2014) parameterization of k. We also add that the absence of wind at night helps explain why fluxes were nearly zero. This has been incorporated into the last paragraph of the Discussion (Lines 389–404).
Line 340 – 342 - In all the studyes wind variability at night is always considered, pCO2 variability is neglected if pCO2 is not measured by authonomous instruments. Here the main difference between day and night is the wind velocity.
We appreciate the reviewer’s remark and agree that wind variability is the key difference between day and night in our dataset. Our intention was not to downplay this, but to emphasize that, since nocturnal fluxes were nearly zero, excluding them can lead to an overestimation of daily means. In the revised Discussion (Lines XX–XX), we have rephrased this point to make it more straightforward: wind remains the dominant driver, but our results illustrate that considering both day and night periods provides a more balanced estimate of diel air–sea CO₂ exchange.
Citation: https://doi.org/10.5194/egusphere-2025-2090-AC2
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AC2: 'Reply on RC1', Ander López, 19 Sep 2025
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RC2: 'Comment on egusphere-2025-2090', Anonymous Referee #2, 23 Jul 2025
Lopez Puerta et al describe the results of a short field campaign examining physicochemical parameters in the surface microlayer and underlying waters of the Croatian coast near Sibenik in the Middle Adriatic Sea. They detail differences in temperature , salinity, and pH that they attribute to changes in solar radiation and metabolic activity. Changes in CO2 fluxes during day and night are attributed to changes in wind speeds and buoyancy fluxes. The SML and controls on its various physical and biogeochemical parameters are important for a variety of reasons including the air-sea exchanges that are the focus of this work. The subject of this paper is, therefore, of interest to the air-sea biogeochemical community. However, the paper suffers from deficiencies that must be considered fully in a revised manuscript prior to its acceptance. My primary concerns have to do with a lack of methodological details and a failure to consider explanations for patterns observed in the data. Specifically, the authors need to address the potential effects of tidal mixing on their data. I detail several of these deficiencies below:
General Comments:
- what are the uncertainties in the temperature, pH and salinity measurements collected using the S3 sampler? The differences being discussed between night and day, SML and ULW, and over short timescales are quite small. Similarly, what is the propagated uncertainty in the sigma-T, pH-T25, and pCO2 calculations. One must know the uncertainties in the measurements to understand whether the fluctuations displayed in figures 5 and 6 (as just two examples of many) are relevant.
- pCO2 data from the Mauna Loa observatory does not seem relevant for the calculation of fluxes in the Mediterranean.
- More information is needed on the sampling location and environmental conditions at the time of sampling. Did the S3 move? Was it deployed in exactly the same location the entire 6 days? A better description of deployment details is needed. What is the water depth at the sampling location? Was there rainfall preceding or during the sampling event? What is the tidal range in the sampling location? What is the typical salinity range at the site (and how does this vary daily due to tides?)?
- Tides: I was surprised that the potential influence of tides on the diurnal parameter variations was never discussed given that the sampling location is described as being on the Croatian coast and appears to be at the mouth of the Krka River estuary where even microtidal tides could influence the salinity, CO2, temperature, pH parameters the authors are measuring. The authors should provide text and/or analysis demonstrating the degree to which tidal mixing of water masses does or does not contribute to the observed variations. To what extent could variations in tides influence the data in Figures 3 and 4, for example? Overlaying the tidal cycle on the graphs in Figure 3 could be very instructive and useful for providing support for or against diurnal-nocturnal versus tidal controls.
Specific Comments:
- lines 303-307 - the authors note that the Krka River normally has low discharge in summer months, but what were the discharge conditions during the time of sampling? Presumably, there are at least precipitation data for that time period, if not discharge data for the river. Those data will be effective for justifying their argument.
Lines 335-336 - why does the lack of wind which forces CO2 fluxes to near 0 demonstrate the need for gas transfer parameterizations with an intercept? While this may be true, the justification is not clear in the argument being made here.
Lines 340-342 - can the authors determine the degree to which the physical and biogeochemical differences in the SML contribute to the differences in the estimated CO2 fluxes (as opposed simply to the wind speed differences)? It seems this could be calculated using a sensitivity analysis which would demonstrate which parameters control these differences in CO2 fluxes between day and night. That type of analysis would place the importance of the diurnal-nocturnal differences in the physical and biogeochemical parameters into proper context.
- Note that 'night' is spelled incorrectly in tables 1 and S2
Citation: https://doi.org/10.5194/egusphere-2025-2090-RC2 -
AC1: 'Reply on RC2', Ander López, 19 Sep 2025
Comments
Response
My primary concerns have to do with a lack of methodological details and a failure to consider explanations for patterns observed in the data. Specifically, the authors need to address the potential effects of tidal mixing on their data.
We thank the reviewer for all the valuable suggestions. The Methods section has been revised to provide additional detail on the study site, deployment strategy, variables measured, and environmental conditions. We also included a general explanation of why tidal effects were not considered in the study. Specific details and clarifications are provided in the responses to the following, more specific comments.
what are the uncertainties in the temperature, pH and salinity measurements collected using the S3 sampler? The differences being discussed between night and day, SML and ULW, and over short timescales are quite small. Similarly, what is the propagated uncertainty in the sigma-T, pH-T25, and pCO2 calculations. One must know the uncertainties in the measurements to understand whether the fluctuations displayed in figures 5 and 6 (as just two examples of many) are relevant.
We appreciate the reviewer’s attention to the uncertainties associated with the S3 measurements and their impact on the interpretation of diel variability.
First, regarding the uncertainties of the sensors, the precision of the temperature, salinity, and pH measurements is now explicitly provided in the Methods section and in Table 1. The pH sensor is reported on the total scale with an accuracy of ±0.005 pH units. In contrast, the precision of the temperature and salinity sensors is ±0.1 °C and ±0.2%, respectively.
Second, concerning the propagated uncertainties in derived variables (σ-t, pHT25, and pCO₂), we have now added a description in the Methods section indicating that these uncertainties were estimated based on the sensor precisions and the measurement errors of DIC and TA. Importantly, the observed diel fluctuations in temperature, salinity, and pHT25 (e.g., changes of ~0.28 °C, 0.30 g kg⁻¹, and 0.016 pHT25 units over 3–5 min intervals) are substantially larger than the associated measurement uncertainties. Therefore, the reported differences between day and night, SML and ULW, and over short timescales are robust and exceed the detection limits of the instrumentation.
These clarifications directly address the reviewer’s concern regarding whether the fluctuations displayed in Figures 5 and 6 are relevant relative to measurement uncertainty.
pCO2 data from the Mauna Loa observatory does not seem relevant for the calculation of fluxes in the Mediterranean.
We appreciate the reviewer’s remark. We agree that the Mauna Loa data are not suitable for flux calculations in a Mediterranean context. To address this, we now use atmospheric pCO₂ data from the ICOS Lampedusa station (di Sarra et al., 2025), which provides representative values for the region. The monthly mean for August 2020 was used to calculate ΔpCO₂ during the campaign. This substitution improves the accuracy and regional relevance of our flux estimates. The corresponding changes have been implemented in the Methods section (Lines 160–166) and applied consistently throughout the results and figures.
More information is needed on the sampling location and environmental conditions at the time of sampling. Did the S3 move? Was it deployed in exactly the same location the entire 6 days? A better description of deployment details is needed. What is the water depth at the sampling location? Was there rainfall preceding or during the sampling event? What is the tidal range in the sampling location? What is the typical salinity range at the site (and how does this vary daily due to tides?)?
We appreciate the reviewer’s request for additional information. The Methods section has been revised to clarify the deployment strategy. The S3 was deployed six times per diel cycle, moving along short transects but treating the sampling location as a single point due to minimal spatial variability. Each deployment lasted 30–45 minutes, during which sensors recorded temperature, conductivity, and pH from both SML and ULW every 30 seconds. The catamaran was remotely piloted and carried an automated water sampler for collecting discrete samples of ~15 L for inorganic carbon analysis.
Environmental conditions were typical for the region during the summer season, as reported in previous studies in nearby areas (cited in lines 94-102). Furthermore, precipitation averaged 1.4 mm during the first 15 days of August, and there was none during the campaign (Croatian Meteorological and Hydrological Service, 2020). (Croatian Meteorological and Hydrological Service, 2020). Tidal ranges were also small, ranging from 0.2 to 0.5 m (Cukrov, 2024), resulting in minimal currents and stable stratification. This environment provided ideal stable conditions for assessing the daily variability of SML and ULW parameters with minimal interference from precipitation or tides (discussed in more detail in the following comment).
Tides: I was surprised that the potential influence of tides on the diurnal parameter variations was never discussed, given that the sampling location is described as being on the Croatian coast and appears to be at the mouth of the Krka River estuary, where even microtidal tides could influence the salinity, CO2, temperature, and pH parameters the authors are measuring. The authors should provide text and/or analysis demonstrating the degree to which tidal mixing of water masses does or does not contribute to the observed variations. To what extent could variations in tides influence the data in Figures 3 and 4, for example? Overlaying the tidal cycle on the graphs in Figure 3 could be very instructive and useful for providing support for or against diurnal-nocturnal versus tidal controls.
We thank the reviewer for bringing this issue to our attention. The Krka River estuary is micro-tidal, with tidal ranges of only 0.2–0.5 m (Cukrov, 2024), resulting in minimal tidal currentsDuring the sampling period, mean precipitation amounted to 1.4 mm for the period preceding the campaign (Croatian Meteorological and Hydrological Service, 2020), resulting in limited variation in river flow. Additionally, groundwater inflows during dry periods, such as summer, are minimal, ranging from 0.19 to 0.31 m³/s (Liu et al., 2019). Consequently, tidal mixing and precipitation-driven river flow are expected to have a negligible influence on the observed diurnal variability of temperature, salinity, pH, and pCO₂. Therefore, these day–night variations primarily reflect local near-surface processes, including surface heating, evaporation, and small-scale turbulence, rather than vertical mixing induced by tides or river discharge.
It is essential to note that the variability we observed follows a diurnal cycle (24 hours) rather than a semi-diurnal cycle (12 hours), further supporting the notion that the observed patterns are driven by surface forcing processes rather than tides. Our approach is also consistent with studies conducted before our experiment on the Croatian coast. Specifically, Stolle et al. (2020) conducted a similar diurnal study in Jade Bay, Germany, where the influence of tides was strong; therefore, the research group decided to replicate the study in a Mediterranean region (characterized by microtidal conditions) to minimize tidal interference. This supports our interpretation that the diurnal patterns we report arise from local environmental processes, rather than tidal forcing.
Lines 303-307 - the authors note that the Krka River normally has low discharge in summer months, but what were the discharge conditions during the time of sampling? Presumably, there are at least precipitation data for that time period, if not discharge data for the river. Those data will be effective for justifying their argument.
We appreciate the reviewer’s suggestion. We have now clarified in the revised manuscript that discharge from the Krka River is generally reduced during the summer months, which is consistent with previous observations in this estuary (Frka et al., 2009; Marcinek et al., 2020). During our sampling period (10–15 August 2020), precipitation was minimal (1.4 mm),as reported by the Croatian Meteorological and Hydrological Service (2020), resulting in negligible short-term fluctuations in river discharge. Moreover, submarine groundwater discharge in the area is known to contribute only a minimal volume (0.19–0.31 m³ s⁻¹) compared to the annual mean river discharge (Bužančić et al., 2016; Marcinek et al., 2020). Together, these hydrological conditions confirm that river inputs and precipitation-driven variability had no significant effect on the salinity and carbonate system parameters observed during our study. The updated manuscript text now includes this clarification.
Lines 335-336 - why does the lack of wind which forces CO2 fluxes to near 0 demonstrate the need for gas transfer parameterizations with an intercept? While this may be true, the justification is not clear in the argument being made here.
We thank the reviewer for this remark. We agree that our dataset alone cannot demonstrate the need for an intercept in parameterisations of k. To clarify this, we have revised the sentence in the Discussion to indicate that our observations are consistent with previous suggestions in the literature (Ribas-Ribas et al., 2019), rather than presenting it as a conclusion from our data.
Lines 340-342 - can the authors determine the degree to which the physical and biogeochemical differences in the SML contribute to the differences in the estimated CO2 fluxes (as opposed simply to the wind speed differences)? It seems this could be calculated using a sensitivity analysis, which would demonstrate which parameters control these differences in CO2 fluxes between day and night. That type of analysis would place the importance of the diurnal-nocturnal differences in the physical and biogeochemical parameters into proper context.
While a sensitivity analysis would indeed be the ideal approach to disentangle the relative contributions of physical and biogeochemical differences in the SML from those driven by wind speed, our dataset does not provide sufficient resolution to support such an analysis in a statistically robust way. The primary objective of this study is rather to illustrate the observed variability and, most importantly, to highlight the bias introduced when nocturnal data are excluded. We agree that a more detailed quantification of parameter control would be valuable, and we plan to address this in future studies with larger datasets. In the revised Discussion (lines 395–4040), we now also emphasize that SML properties, such as enhanced CO₂ solubility under slightly cooler and fresher conditions and reduced turbulence at night, contribute to the observed differences in fluxes.
Note that 'night' is spelled incorrectly in tables 1 and S2
We have changed the text accordingly.
Citation: https://doi.org/10.5194/egusphere-2025-2090-AC1
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AC1: 'Reply on RC2', Ander López, 19 Sep 2025
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- 1
The paper presents the results of a field experiment investigating diel variability in the marine carbonate system within the sea-surface microlayer (SML) in the Middle Adriatic, along the Croatian coast. An instrumented catamaran collected continuous measurements of temperature, salinity, and pH over three complete 24-hour cycles and took discrete seawater samples to analyze DIC, TA, and nutrient concentrations, both in the SML and at 1 m depth (ULW).
These data were then used to calculate CO₂ partial pressure (pCO₂) and pH on the total scale at 25 °C (pHT25). The authors used the calculated pHT25, together with temperature, to correct pH values obtained from the pH electrode. The derived pCO₂ values were subsequently used to estimate CO₂ fluxes over the daily cycle.
The results showed some statistically significant differences (p < 0.05) between daytime and nighttime values of temperature, salinity, and pHT25 and/or SML and ULW. These variations are then discussed, taking into account several influencing factors. Differences in CO₂ fluxes between day and night are also highlighted, underscoring the importance of considering the full diel cycle in air–sea CO₂ flux estimations.
The paper addresses an important aspect for improving air–sea CO₂ flux calculations, but it suffers from several weaknesses, both in the methodological description and in the discussion of the results.
The introduction focuses primarily on carbonate chemistry and the relevance of pCO₂ measurements, without adequately introducing the unique characteristics of the SML and its relevance for air–sea CO₂ fluxes (e.g., see the review by Cunliffe et al., 2013: https://doi.org/10.1016/j.pocean.2012.08.004). A more comprehensive and updated bibliographic foundation is needed. For example, in line 40, Cantoni et al. (2012) does not present trends in acidification but rather biogeochemical drivers of pH variability. Doney’s work is a milestone, but more recent references are necessary. Similarly, in line 52, Cantoni et al. (2016) does not mention the SML.
The methods section is unclear. It lacks essential information needed to understand what was done, where, and on how many samples the study is based. The system used for data acquisition is not described, and there is no introduction to the study site or description of where the data were collected. See detailed comments in the manuscript.
Regarding carbonate system parameters, pH was measured continuously, but no details are provided about the electrode, calibration procedures, or accuracy. DIC and TA were measured using state-of-the-art methods on a limited number of discrete samples, as reported in Table 1: 3–4 samples during the day and 1–2 at night. These data were then used to calculate pCO₂ and pH at 25 °C. An estimate of the uncertainty associated with these calculations is necessary before discussing the results.
Using atmospheric pCO₂ values from the Mauna Loa Observatory is not appropriate for estimating air–sea CO₂ fluxes in the Mediterranean. Data from the ICOS station at Lampedusa or other regional/interpolated products should be used instead.
The data discussion is weak. Various hypotheses are proposed to explain the observed variability, but these are not supported by further analysis or robust conclusions. For instance, in line 285 and following, the effect of evaporation on SML cooling is introduced, but the conclusion simply states that this affects pHₜ₂₅, without explaining whether it increases or decreases, and by which mechanisms. Other processes are mentioned without clarification. The overall conclusion is that "it is complicated, with an interplay of several factors," but this does not advance the current understanding.
One of the main conclusions is the importance of including nighttime in the study of air–sea CO₂ fluxes. Wind speed and ΔpCO₂ are the primary variables controlling these fluxes, with wind dependence incorporated into the parameterization of “k” (line 131; Wanninkhof, 2014). Wind speeds were lower during the night (line 174), which would be expected to result in lower fluxes. However, the authors do not consider this aspect, and the relevance of diel ΔpCO₂ variability is not adequately discussed.
Further specific comments are provided in the annotated manuscript.
Overall, the paper, in its current form, is not suitable for publication in Ocean Science. However, if the authors are able to significantly improve the methodological section and strengthen the data analysis and discussion, the manuscript could be reconsidered for publication upon resubmission.