In situ Determination of Nitrate and Hydrogen Sulfide in the Baltic Sea Using an Ultraviolet Spectrophotometer

Evaluating the health status of marine ecosystems becomes ever increasingly important especially against the backdrop of rising pressures from human activities. This is true especially for coastal seas such as the Baltic Sea that is surrounded by highly industrialized countries. Nutrients and pollutants such as nitrate and hydrogen sulfide, which have a major impact on ecosystem functioning, are two of several key environmental indicators for assessing the status of natural waters, and therefore of considerable interest. The frequency and the spatial coverage of the nitrate and hydrogen sulfide measurements are currently limited by the cost of the laboratory analysis and personnel. Optical in situ sensors can help to overcome this challenge by allowing reagentless and fast detection of dissolved chemical species. A chemical-free optical sensor has been used for direct and simultaneous measurements of both key parameters, and the results were compared with traditional methods. The data were collected during an observational program conducted in the Baltic Sea in February 2018. We used the OPUS UV spectral sensor, which was deployed for the first time in coastal waters, in combination with a deep-sea telemetry system to enable near-real time measurements during CTD profiling. Data processing was carried out using a multiple linear regression procedure. Measurements from both OPUS and on-board analysis were in good agreement. The results showed, that in situ UV-VIS spectrophotometry provides the capability to determine the concentration distributions of nitrate and hydrogen sulfide in the brackish waters of the Baltic Sea.

Introduction

Throughout the world, agriculture, fossil-fuel combustion, and other human activities are leading to increasing levels of reactive nitrogen in the environment (Galloway et al., 2003; Gruber and Galloway, 2008). As a result, human health and ecosystem functions increasingly suffer from the effects of eutrophication and hypoxia, both at regional and global scales (Diaz and Rosenberg, 2008; Conley et al., 2009, 2011; Villnäs et al., 2013). The Baltic Sea is a semi-enclosed sea surrounded by highly industrialized riparian states and is particularly sensitive to anthropogenic impacts and natural fluctuations (Matthäus, 1995).

High reactive nitrogen levels cause increased biomass production (Falkowski et al., 1998) and thus increased sedimentation of organic material. Subsequent remineralization leads to bottom water oxygen deficiency, increased sulfate reduction and ultimately to the production of hydrogen sulfide (H₂S), which is highly toxic to most organisms (Gray et al., 2002). In the Baltic Sea, as deep water renewal is hampered by the strong pycnocline and submarine sills, total sulfide (∑S²⁻ = H₂S + HS⁻ + S²⁻) accumulates in the water column and can reach concentrations of up to 200 μM. These stagnation periods can last for many years and are only interrupted by inflow events from the North Sea under certain meteorological conditions (Schinke and Matthäus, 1998).

Nitrate (${\text{NO}}_3^{-}$), as the major component of reactive nitrogen as well as H₂S, are therefore of great importance for the ecological state of the Baltic Sea and thus are monitored by the coastal countries, which have adopted the Helsinki Convention for the Protection of the Marine Environment of the Baltic Sea in order to abate eutrophication by reducing nutrient loads from point and non-point sources (Backer et al., 2010). Many methods for the detection of ${\text{NO}}_3^{-}$ (Moorcroft et al., 2001) and H₂S (Lawrence et al., 2000) have been developed, but in most marine laboratories the determination of both compounds is usually carried out via simple colorimetric measurements (Grasshoff et al., 2009). The frequency and the spatial coverage of these measurements are currently limited by the cost of the laboratory analysis and personnel. Furthermore, the sampling process and preparation of the mostly toxic reagents is time consuming and involves multiple sources of error. However, with the help of in situ sensors, it is possible to reduce the working time as well as contamination and altering of the sample. In addition, in situ sensors have a small size, low weight and relatively low energy consumption, and therefore are suitable for being deployed on moorings (Collins et al., 2013; Sakamoto et al., 2017), floats (Johnson et al., 2013, 2017; D'Ortenzio et al., 2014; Pasqueron de Fommervault et al., 2015), towed vehicles (Pidcock et al., 2010) or autonomous underwater vehicles (Johnson and Needoba, 2008). In situ sensors are thus helping to bridge the gap between large-scale but non-specific remote observations of satellites limited to the surface waters and highly sophisticated and specific laboratory analysis from discrete water samples (Zielinski et al., 2009).

In general, there are three different types of in situ sensors that can be used for ${\text{NO}}_3^{-}$ measurements: (1) wet chemical analyzers, (2) optical UV sensors, and (3) ion selective electrodes (ISEs). Each of these methods has its own advantages and disadvantages. Wet chemical analyzers such as the WIZ probe (Vuillemin and Sanfilippo, 2010) or Lab-on-chip devices (Beaton et al., 2012) are using chemical reagents and thus produce high maintenance toxic waste. Furthermore, operating lifetime of those analyzers is strongly dependent on reagent stability. On the other side, they can be calibrated in situ and thus have small uncertainty of measurement. However, the preparation of stable standard solutions for H₂S and ${\text{NO}}_3^{-}$ measurements is difficult as the shelf life of these standards is limited. By contrast, optical UV sensors such as Nitratax (Hach Lange GmbH, Germany), ISUS/SUNA (Johnson and Coletti, 2002; Johnson et al., 2006; MacIntyre et al., 2009) (Satlantic, Canada), or ProPS/OPUS (Zielinski et al., 2007; Prien et al., 2009) (TriOS GmbH, Germany) do not require any chemical reagents but are influenced by optical/ionic interferences including bromide (Br⁻), chloride (Cl⁻), turbidity and water color. ISEs such as NISE (Hach Lange GmbH, Germany) and EXO (YSI Inc., USA) are not influenced by turbidity and water color, but deteriorate quite rapidly when used under environmental conditions since the sensor molecules in the membrane change or are leached out. Therefore, they are often subject to significant drift and require regular re-calibration (Moorcroft et al., 2001; Le Goff et al., 2002). UV sensor technology is therefore used most frequently and has been increasingly used for ${\text{NO}}_3^{-}$ measurements in a variety of environments such as rivers (Pellerin et al., 2009; Wade et al., 2012; Feng et al., 2013; Aubert and Breuer, 2016; Chappell et al., 2017; Kunz et al., 2017), groundwaters (Huebsch et al., 2015), coastal waters (Zielinski et al., 2011; Frank et al., 2014), open ocean waters (Omand and Mahadevan, 1966; Johnson, 2010; Ascani et al., 2013) and hydrothermal vents (Le Bris et al., 2000).

The aims of this study were to validate and optimize an optical in situ method for the precise and accurate simultaneous measurement of ${\text{NO}}_3^{-}$ and HS⁻ in brackish waters of the Baltic Sea. We used the OPUS UV spectral sensor (TriOS, Oldenburg, Germany), which was deployed for the first time in coastal waters, allowing improved observations of both compounds. Near-real time measurements and online sensor control was realized by using a deep-sea telemetry system integrated into the conductivity-temperature-depth (CTD) rosette sampler. Furthermore, detailed protocols have been developed for both sensor calibration and data evaluation. Finally, results were confirmed by comparison with conventional measurements made by an independent laboratory based method.

Materials and Methods

Instrumentation

During CTD profiling, high-frequency ${\text{NO}}_3^{-}$ measurements were conducted using an OPUS UV spectral sensor (TriOS GmbH, Germany) deployed on a CTD-rosette sampler. The sensor is highly portable, light weight (titanium; 2 kg) and has moderate power consumption (< 8 W). The system is approximately 470 mm long with a diameter of 48 mm, has an open optical path length of 10 mm and can be deployed to a maximum depth of 300 m. It utilizes a xenon flash lamp and a 256 channel high-end miniature spectrometer (MMS, Zeiss, Jena, Germany) that covered the spectral range 200– 360 nm. The light source intensity of the xenon lamp is monitored by a reference photodiode and changes caused by temperature and aging phenomena are taken into account by an internal function of the sensor software. Measurements were carried out at 20 s intervals using an integration time of 256 ms. The lowering speed of the rosette sampler of 0.3 m/s thus resulted in a vertical resolution of 6 m and a smearing of the signal of 0.08 m for the OPUS measurements. Time synchronization was realized via coordinated universal time (UTC), which was used by all in situ instruments and allowed for the direct comparison of OPUS data with CTD measurements. A segmented flow analyzer (FlowSys, Alliance Instruments, Austria) for on-board spectrophotometric detection of ${\text{NO}}_3^{-}$ was used as a reference method. In case of ∑S²⁻, collected water samples were analyzed by the methylene blue method (Cline, 1969) and the resulting concentration values were used for sensor validation. Limit of detection for ${\text{NO}}_3^{-}$ and ∑S²⁻ was 0.1 μM and 1 μM, respectively.

Online control of the sensor was realized by using a deep-sea telemetry system (Sea & Sun Technology GmbH) integrated into the CTD rosette sampler. Hydrographic data were collected using a standard CTD system (Model SBE911Plus; Sea-Bird Electronics Inc., USA). Turbidity was measured at 700 nm using the ECO-FLNTU sensor (WETLabs, USA). Profiling was carried out with active heave compensation using a special hydraulic crane winch (Krüger, S., and Ruickoldt, J., inventors; Leibniz-Institute for Baltic Sea Research Warnemünde, assignee. Measurement of measured quantities and/or sampling under water. Germany patent DE 102014201815. 2014 Jan 31). All measurements were stored in the database of the Leibniz Institute for Baltic Sea Research (IOWDB). Free registration is required for open access to IOWDB data (https://odin2.io-warnemuende.de/registration).

Field Deployments

Field studies were conducted during a RV Elisabeth Mann Borgese monitoring cruise in the Baltic Sea (Cruise No.: EMB175; from 30.01.2018 to 09.02.2018), which is the largest brackish water ecosystem on earth (average depth: 52 m; maximum depth: 459 m, surface area: 4.2 × 10⁵ km², volume: 22 × 10³ km³ (Seifert et al., 1995; HELCOM, 2002). It is a semi-enclosed, non-tidal estuary consisting of several sub-basins and sills. The deep water of the central basins can become temporary or permanently euxinic (anoxic and sulfidic) due to biodegradation processes (Piker et al., 1998). In this area, stratification and topographic features (e.g., sills, trenches) have a great impact on hydrodynamics with respect to mixing and water renewal processes (Matthäus and Schinke, 1999; Elken and Matthäus, 2008). Ventilation of the deeper layers is occurring only under specific meteorological conditions (strong and long lasting easterly winds followed by strong and long lasting westerly winds) which then cause an inflow of high saline and oxygen-rich water masses from the North Sea (Schinke and Matthäus, 1998). The last strong Major Baltic Inflow (MBI) event that led to a renewal of bottom waters in many parts of the Baltic Sea occurred in December 2014 (Mohrholz et al., 2015). During our study, however, the development of a new stagnation period could be observed (Leibniz Institute for Baltic Sea Research, 2016). The field studies included three sensor deployments at multiple sites (Figure 1A) each representing a certain area (Bornholm Basin, Eastern Gotland Basin, Western Gotland Basin). All of these stations belong to the Baltic Proper, which is most affected by eutrophication and hypoxia. In addition, changing environmental conditions (e.g., decreasing salinity and increasing H₂S concentrations) from the Bornholm Basin over the Eastern Gotland Basin to the Western Gotland Basin (Figure 3) allowed us to more accurately investigate the suitability of the applied method.

FIGURE 1

Figure 1. (A) Map of the study area including the locations of OPUS deployments indicated by white stars; 1 = Arkona Basin, 2 = Bornholm Basin, 3 = Gulf of Gdansk, 4 = Eastern Gotland Basin, 5 = Northern Baltic Proper, 6 = Western Gotland Basin. (B) UV-spectra of standard solutions (${\text{c}}_{N{O}_3^{-}}=10$ μM; ${\text{c}}_{B{r}^{-}}=247$ μM; ${\text{c}}_{C{l}^{-}}=125$ mM; ${\text{c}}_{HC{O}_3^{-}}=1615$ μM; ${\text{c}}_{H{S}^{-}}=45$ μM) measured in the laboratory by using the OPUS sensor.

Optical Measurements

Interfering Ions

The Baltic Sea, like all natural waters, is a demanding environment for optical in situ measurements due to interfering ions which have high absorbances in the same wavelength range as ${\text{NO}}_3^{-}$ and HS⁻. Interfering ions include Br⁻ (Ogura and Hanya, 1966), Cl⁻ (Finch et al., 1998), nitrite (${\text{NO}}_2^{-}$) (Johnson and Coletti, 2002), hydrogen carbonate (${\text{HCO}}_3^{-}$) (Kröckel et al., 2011), and certain functional groups of the dissolved organic carbon (DOC) pool (Stedmon and Nelson, 2014). Sample absorption spectra are thus always a superposition of the absorption spectra of several different species. Hence, a mathematical approach has to be applied in order to decompose the obtained spectra. For the deconvolution and subsequent calculation of the analyte concentrations, a multiple linear regression method (henceforth referred to as MLR) was chosen (Thomas and Gallot, 1990) and implemented in the MATLAB environment (Mathworks, R2014a). A detailed description of this procedure is given in the subsection “Data Processing.”

For the regression to work, it needs the individual absorption spectra of all ions involved. For this reason, standard solutions of typical Baltic Sea concentrations were prepared for all relevant ions (${\text{NO}}_3^{-}$, HS⁻, Br⁻, Cl⁻, ${\text{HCO}}_3^{-}$) and absorption spectra were measured in the laboratory by using the OPUS sensor. An exception is CDOM (colored dissolved organic matter), the optically active part of DOC, since its composition is widely unknown and highly variable. It should be noted at this point that different approaches to the treatment of CDOM interferences exist in the literature (Johnson and Coletti, 2002; Sakamoto et al., 2009; Zielinski et al., 2011). Usually, a simple linear or quadratic function is used during data processing to take into account background signals caused by CDOM. However, the influence of CDOM on OPUS measurements will be discussed later in conjunction with our findings. The resulting absorption spectra of the standard solutions are shown in Figure 1B. Br⁻ represents the main interfering ion, followed by Cl⁻ and ${\text{HCO}}_3^{-}$. Nitrite was neglected as concentrations found during our study were below 0.2 μM. In the case of HS⁻, the pH of the standard solution was adjusted to a pH of 7.3 by using a KH₂PO₄/Na₂HPO₄ buffer solution to provide pH conditions similar to the in situ conditions at the study area, as the dissociation of H₂S is pH-dependent (Millero et al., 1988).

Temperature Effect

Temperature dependencies must be taken into account when measuring calibration spectra, as otherwise accuracy of the regression results decreases (Zielinski et al., 2007). For this reason, temperature studies for the standard solutions of ${\text{NO}}_3^{-}$, HS⁻, Br⁻, and Cl⁻ were made. Standard solutions were first cooled down by using an ice bath and then slowly warmed up by putting the ice bath aside. While slowly warming up, the solutions were then pumped through the OPUS sensor by using a flow cell in which the measurements were carried out every 20 s. Temperature measurements were realized by using an Arduino-controlled DS18B20 temperature sensor with a sensitivity of 0.5°C mounted in the flow cell.

The results can be seen in Figure 2A, where absorbances at a wavelength of 210 nm are plotted as a function of temperature. As can be seen from this figure the Cl⁻ absorbance at 210 nm is rather insensitive to temperature changes, while Br⁻ and HS⁻ absorbances at this wavelength are strongly sensitive to temperature. For Br⁻ and Cl⁻ this interrelationship has already been demonstrated by other workers (Zielinski et al., 2007; Sakamoto et al., 2009) and is probably due to the interaction of the dissolved ions with water, i.e., due to a charge transfer to solvent complex (Jortner et al., 1964). Similar considerations could be made for HS⁻, but as far as we know there have been no studies on its photochemistry, yet. In fact, and to the best of our knowledge, our data is showing for the first time the temperature dependence of HS⁻ absorbance in the deeper UV region. In contrast, the ${\text{NO}}_3^{-}$ absorbance shows no temperature dependence at all owing to the π to π* transition, which occurs only within the molecule and without any solvent interaction (Mack and Bolton, 1999).

FIGURE 2

Figure 2. (A) OPUS absorbance of Br⁻, HS⁻, ${\text{NO}}_3^{-}$, and Cl⁻ at 210 nm wavelength plotted as a function of temperature. Equations for the regression lines are: Br⁻ = 0.007*x+0.314 (R² = 0.98), HS⁻ = 0.005*x+0.154 (R² = 0.90), ${\text{NO}}_3^{-}=0.0001*$x+0.087 (R² = 0.03), Cl⁻ = 0.001*x+0.010 (R² = 0.47). (B) Sample absorption spectrum measured at station TF245 at 4.1 °C (solid line) and UV-spectra resulting from the multiple linear regression procedure. Added up “sum of spectra” and “poly_4” give the solid line.

Data Processing

The absorbance at each pixel of the detector array was determined from following equation: A(λ) = -log((I_λ−I_d)/(I_{λ, 0}−I_d)), where I_λ is the detector current (counts) after light passing through the sample, I_{λ, 0} detector current after light passing Milli-Q water (resistance ≥ 18 MΩcm⁻¹, Merck Millipore, Bellerica, USA) as reference and I_d the detector current without light source (dark current measurement). Each time a spectrum of a calibration solution was measured, a Milli-Q water spectrum was recorded to determine I_{λ, 0}.

The following equations, using the example of ${\text{NO}}_3^{-}$, illustrate the steps taken to obtain ${\text{NO}}_3^{-}$ and HS⁻ concentrations respectively.

$\begin{array}{cc}{A}_1=A_{0,\text{sample}}-\left(f_{{\text{Cl}}^{-}}\cdot A_{{\text{Cl}}^{-}}\right)-\left(f_{{\text{HCO}}_3^{-}}\cdot A_{{\text{HCO}}_3^{-}}\right)& (1)\end{array}$

$\begin{array}{l}{P}_{\left({\text{NO}}_3^{-},{\text{Br}}^{-},\text{poly}4\right)}=regress\left(A_1,X\right),\\ \text{\hspace{1em}where X}=\left[{\text{A}}_{{\text{NO}}_3^{-}},{\text{A}}_{{\text{Br}}^{-}},{\text{A}}_{\text{poly}4}\right]& (2)\end{array}$

$\begin{array}{cc}{c}_{{\text{NO}}_3^{-},\text{sample}}=p_{{\text{NO}}_3^{-}}\cdot c_{{\text{NO}}_3^{-},\text{standard}}& (3)\end{array}$

First, a temperature corrected Cl⁻ and a ${\text{HCO}}_3^{-}$ spectrum were subtracted from the respective sample absorption spectrum as both components are potential interferents (see Equation 1). They were not included in the MLR procedure but subtracted from the sample spectrum in order to reduce the number of unknowns in the subsequent regression. As the salinity of the sample differs from the salinity of the Cl⁻ calibration spectrum (S = 8) a simple correction (multiplication by a factor) was carried out using salinity data from the CTD probe. The ${\text{f}}_{C{l}^{-}}$-values so were obtained by dividing CTD salinity by 8, since the Cl⁻ calibration solution had a salinity of 8. In the case of the ${\text{HCO}}_3^{-}$ calibration solution (${\text{c}}_{HC{O}_3^{-}}=1,615$ μM) multiplication factors were set to 1 (< 60 m), 1.1 (> 60 and < 80 m), and 1.2 (> 80m), to provide total CO₂ conditions similar to the in situ conditions at the study area (Beldowski et al., 2010). In other environments, such as the North Atlantic, the multiplication factors would have to be chosen differently, since the total CO₂ concentrations differ from those of the Baltic Sea (Takahashi, 1981). Calibration spectra (absorbances) of ${\text{NO}}_3^{-}$, HS⁻, and Br⁻ were then combined to form a matrix M (henceforth referred to as calculation group) that was used in the MLR procedure (see Equation 2). Furthermore, a poly_4 spectrum (λ⁻⁴) was added to the calculation group in order to take into account that scattered light can also contribute to the sample absorption signal.

As we will see later in the discussion part, other non-scattering components can also be added to the poly_4 spectrum during the regression, if the shape of the spectra are not very different from each other. Finally, the MLR (210– 230 nm wavelength range) was carried out depending on the dissolved oxygen concentrations (O₂) measured at each depth. When O₂ was present (> 1 μM) the calculation group included Br⁻, poly_4 and ${\text{NO}}_3^{-}$. In contrast, when O₂ was absent (< 1 μM), the calculation group included Br⁻, poly_4, and HS⁻. All calibration spectra within the calculation group were selected from the temperature study to be as close as possible to the in situ temperature conditions. This is of considerable importance for Br⁻ and HS⁻ as can be seen from Figure 2A. Polynomial coefficients (p) obtained from MLR were then used for calculating the ${\text{NO}}_3^{-}$, HS⁻, and Br⁻ concentrations as well as the poly_4 contribution (see Equation 3).

Results

During a monitoring cruise in the Baltic Sea in February 2018, in situ measurements were carried out with the OPUS. The OPUS was mounted on the CTD rosette sampler and could be controlled online via a deep-sea telemetry system. The hydrographic data of the measured stations (TF200, TF286, TF245) and the results of the MLR are shown in Figure 3. In addition, summarized results of laboratory and sensor measurements can be found in Table 1. The CTD data (Figures 3A,D,G) indicated a stratified water column with cold, low-saline surface water and warm, saline deep water. O₂, temperature and salinity values were fairly uniform in the surface layer at all three stations due to the winter mixing (TF200: 357 μM, 4.6°C, 7.5; TF286: 358 μM, 4.5°C, 7.3; TF245: 359 μM, 4.1°C, 7.3). Below 50 m depth, the salinity and the temperature increased and reached nearly constant values in the bottom water (TF200: 6.8°C, 17.3; TF286: 6.8°C, 12.8; TF245: 5.6°C, 10.3). In contrast, the O₂ concentrations sharply decreased from 50 m depth so that no O₂ was present in the bottom water of all three stations. In addition, intrusions of O₂-rich water could be located at station TF200 and TF286 at 60 m and 125 m depth, respectively. When O₂ was not present, ∑S²⁻ was determined using the methylenblue method (MBM) as well as the OPUS sensor (Figures 3B,E,H). Concentrations close to the bottom obtained by MBM were 4.3 μM (TF200), 14.6 μM (TF286) and 33.6 μM (TF245). Concentrations of ∑S²⁻ obtained by the OPUS sensor at about the same depths were 5.6 μM (TF200), 16.9 μM (TF286), and 34.3 μM (TF245). Furthermore, ${\text{NO}}_3^{-}$ was measured using a segmented flow analyzer (SFA) and the OPUS sensor (Figures 3B,E,H). At the surface, ${\text{NO}}_3^{-}$ concentrations were consistently high and slowly increasing northwards. Concentrations above 50 m depth obtained by SFA were in average 2.4 μM ± 0.1 μM (TF200), 3.6 μM ± 0.04 μM (TF245), and 3.9 μM ± 0.02 μM (TF286). Concentrations of ${\text{NO}}_3^{-}$ obtained by the OPUS sensor above 50 m depth were in average 2.5 μM ± 0.2 μM (TF200), 3.3 μM ± 0.2 μM (TF245), and 5.9 μM ± 0.2 μM (TF286). ${\text{NO}}_3^{-}$ maxima were observed at station TF200 and station TF286 at 60 m and 125 m depth, respectively, and coincided with above-mentioned O₂ intrusions.

FIGURE 3

Figure 3. Data from the February 2018 cruise. (A,D,G) Vertical profiles of salinity, temperature and O₂ concentration; (B,E,H) Comparison of bottle measured ${\text{NO}}_3^{-}$/∑S²⁻ data and OPUS results.(C,F,I) Theoretical Br⁻ concentrations (calculated using salinity data), Br⁻ concentrations measured by OPUS, turbidity data from CTD measurements (multiplied by 50), and poly_4 results presented as “percentage of sample absorption at a wavelength of 210 nm”.

TABLE 1

Table 1. Summarized results of laboratory and sensor measurements.

Additional parameters (Br⁻, turbidity, and poly_4) are shown in Figures 3C,F,I. Br⁻ was measured with the OPUS sensor but was also calculated from salinity using CTD data whereby conservative behavior was assumed. Turbidity (reported in nephelometric turbidity units or NTU) was measured in parallel with temperature and salinity and was multiplied by 50 for plotting in the figures. In the upper water column turbidity values were rather low. High turbidity was observed especially in the euxinic deep water where O₂ was absent. Furthermore, poly_4 values resulting from the MLR are also shown Figure 3 and are presented as “percentage of sample absorption at a wavelength of 210 nm” in order to show how much of the sample absorbance could not be allocated to any of the calibration spectra included in the calculation group. Poly_4 values were about 24% (TF200), 25% (TF245), and 17% (TF286) in the surface water and 4% (TF200), 8% (TF245), and 4% (TF286) in the bottom water.

Discussion

OPUS and laboratory results were measured at different depths and thus a direct correlation of the concentration data would be inappropriate. Instead, averaged ${\text{NO}}_3^{-}$ concentrations above a depth of 50 m, as presented in the results section were compared for each station. Resulting deviations for ${\text{NO}}_3^{-}$ were 4% (TF200), 8% (TF245), and 51% (TF286). In the case of ∑S²⁻ the bottom water concentrations between bottle data and OPUS data were compared. Deviations found here were 30% (TF200), 2% (TF245), and 14% (TF286). As mentioned above, dissociation of H₂S is pH-dependent and the calibration solution used in this study was buffered to a constant pH of 7.3. Therefore, the reported deviations could be explained by variations in the in situ pH of the study area. However, considering that the highest deviations observed for ${\text{NO}}_3^{-}$ (51%) and ∑S²⁻ (30%), correspond to only 2 and 1.3 μM, respectively, it can be stated that ${\text{NO}}_3^{-}$ and ∑S²⁻ measurements carried out at the Baltic Sea using the OPUS sensor are in satisfactory agreement with those obtained from reference methods. Although, the findings of our study are limited by the small number of measured stations, presented results show that both ${\text{NO}}_3^{-}$ and ∑S²⁻, as important environmental parameters, can be determined in situ, simultaneously and without reagents during classical CTD work, providing near real time readings with sufficient accuracy without time and cost intensive traditional laboratory analysis. That the deconvolution of the sample spectra was successful is also shown by the MLR results of the other parameters that were included in the calculation groups. For instance, OPUS Br⁻ concentrations and theoretical Br⁻ concentrations correspond very well with each other (Figures 3C,F,I). Maximum deviations were found in the bottom water and were only 6% (TF200), 3% (TF245), and 6% (TF286). It should be noted here, that pressure effects on bromide absorbance were neglected in our study because we have worked in shallow waters, but should be taken into account at higher pressures (Sakamoto et al., 2017).

But although ${\text{NO}}_3^{-}$, Br⁻, and ∑S²⁻ concentration data of the OPUS sensor fit very closely with the laboratory and theoretical data and all features of the concentration distributions are reproduced some questions still remain. Figure 3B, for example, shows a sample absorption spectrum from station TF245 at 6 m depth and the results of the deconvolution using the calibration spectra during the MLR. The sum of the ${\text{NO}}_3^{-}$, Br⁻, HCO${}_3^{-}$, Cl⁻, and poly_4 spectrum would give the sample spectrum. The polynomial coefficients provided by the MLR with regard to the light scattering term (poly_4) seem to be remarkable high. This is especially true for the upper water column as can be seen from Figure 3, where up to 25% of the sample absorption is allocated to the poly_4 spectrum.

On the one side, we assume that light scattering actually could be increased by suspended particulate matter (SPM), as certain colloidal fractions can have scattering coefficients significantly greater than pure sea water (Stramski and Woźniak, 2005). On the other hand, we think that absorption fractions of CDOM were added to the poly_4 term during the regression, since we did not add such a calibration spectrum to the calculation groups. This assumption is underpinned by the striking inverse correlation between poly_4 and salinity (Figure 3), as it has also been found for CDOM in other coastal waters (Fichot and Benner, 2011). Although CDOM should be the most relevant parameter at this point, one aspect of future research thus could be to investigate the impact of both the particulate and the dissolved components of organic material on in situ UV measurements. Since the optical properties of CDOM have been found to be empirically related to DOC concentration (Fichot and Benner, 2011) further research could also help to get a better understanding of DOC cycling. This could be of considerable interest, since dissolved organic material (DOM) and DOC, as a major component of the DOM pool, can enhance eutrophication and pollution of natural waters, for instance, by the mobilization of phosphorous and heavy metals (Fest et al., 2008; Ros et al., 2010). Since the aim of the current work was to detect ${\text{NO}}_3^{-}$ and ∑S²⁻, correction for this offset as performed by other workers (Sakamoto et al., 2009; Zielinski et al., 2011) was not carried out.

Although, the findings of our study are clearly limited by the small number of measured stations, the OPUS sensor in combination with deep-sea telemetry allowed in situ determination of ${\text{NO}}_3^{-}$ and ∑S²⁻ in the Baltic Sea, enhancing monitoring data set. This approach increases the simplicity of the determination of both parameters and the speed of data acquisition. Concentration gradients as well as maxima and minima can be determined more accurately as the spatial resolution of the data can be higher than using traditional bottle sampling. The OPUS is capable of resolving ${\text{NO}}_3^{-}$ variability on a scale of 6 m at a CTD lowering speed of 0.3 m/s (OPUS sampling rate: 0.05 Hz). At lower profiling speed the vertical resolution could be even higher. A future cooperation with the manufacturer TriOS (Oldenburg, Germany) could help to further improve the sampling rate. Meanwhile, we have received a new firmware allowing OPUS measurements at a sampling rate of 0.1 Hz which results in 3 m vertical resolution. A relevant step to resolve e.g., steep gradients in the water column.

Finally, it can be concluded that there is a clear need of innovative and cost-effective monitoring (Zielinski et al., 2009; Borja and Elliott, 2013) and using sensors such as OPUS is a smart way of gathering relevant information quickly. Modern oceanographic tools like the instrument described here should be more widely used. This is especially important to identify anthropogenic impact (e.g., in the form of sporadic events) and their consequences for the marine ecosystems. The affected processes can have a wide range of temporal and spatial scales, requiring frequent and distributed observations. Only then can the feedbacks be unraveled and the ecosystem status adequately assessed.

Author Contributions

DM, LR, MP, and RP conceived and designed the experiments. LR, MP, and DM performed the experiments. DM and LR compiled and processed all the field and laboratory data. DS-B, RP, and JW contributed materials, reagents, analysis tools. DM wrote the paper, with edits and contributions from all co-authors. RP, JW, and DS-B directed the study and its scope.

Funding

Parts of this work have been carried out within the BONUS SEAMOUNT project (BMBF 03F0771C).

Conflict of Interest Statement

The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.

Acknowledgments

We thank the captain and the crew of RV Elisabeth Mann Borgese (EMB175). We acknowledge in particular Susanne Schöne and Lars Kreuzer for sampling and conducting on-board measurements of O₂, ∑S²⁻ and ${\text{NO}}_3^{-}$ concentrations. Thanks are due to Siegfried Krüger for his help with the deep-sea telemetry system. Furthermore, the support of Birgit Sadkowiak during the lab work is greatly appreciated. We are thankful for the technical support we experienced from TriOS GmbH (Oldenburg, Germany). DM would also like to thank Anne Köhler for measuring ∑S²⁻ concentrations during the sensor calibration experiments. The authors thank the three reviewers for their detailed and valuable comments that helped improve the manuscript.

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