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<journal-meta>
<journal-id journal-id-type="publisher-id">Front. Mar. Sci.</journal-id>
<journal-title>Frontiers in Marine Science</journal-title>
<abbrev-journal-title abbrev-type="pubmed">Front. Mar. Sci.</abbrev-journal-title>
<issn pub-type="epub">2296-7745</issn>
<publisher>
<publisher-name>Frontiers Media S.A.</publisher-name>
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<article-meta>
<article-id pub-id-type="doi">10.3389/fmars.2024.1363088</article-id>
<article-categories>
<subj-group subj-group-type="heading">
<subject>Marine Science</subject>
<subj-group>
<subject>Original Research</subject>
</subj-group>
</subj-group>
</article-categories>
<title-group>
<article-title>Iron dissolution from Patagonian dust in the Southern Ocean: under present and future conditions</article-title>
</title-group>
<contrib-group>
<contrib contrib-type="author" corresp="yes">
<name>
<surname>Demasy</surname>
<given-names>Cl&#xe9;ment</given-names>
</name>
<xref ref-type="aff" rid="aff1">
<sup>1</sup>
</xref>
<xref ref-type="author-notes" rid="fn001">
<sup>*</sup>
</xref>
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<contrib contrib-type="author">
<name>
<surname>Boye</surname>
<given-names>Marie</given-names>
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<sup>1</sup>
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<contrib contrib-type="author">
<name>
<surname>Lai</surname>
<given-names>Barry</given-names>
</name>
<xref ref-type="aff" rid="aff2">
<sup>2</sup>
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<contrib contrib-type="author">
<name>
<surname>Burckel</surname>
<given-names>Pierre</given-names>
</name>
<xref ref-type="aff" rid="aff1">
<sup>1</sup>
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<contrib contrib-type="author">
<name>
<surname>Feng</surname>
<given-names>Yan</given-names>
</name>
<xref ref-type="aff" rid="aff3">
<sup>3</sup>
</xref>
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<contrib contrib-type="author">
<name>
<surname>Losno</surname>
<given-names>R&#xe9;mi</given-names>
</name>
<xref ref-type="aff" rid="aff1">
<sup>1</sup>
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<contrib contrib-type="author">
<name>
<surname>Borensztajn</surname>
<given-names>Stephan</given-names>
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<sup>1</sup>
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<name>
<surname>Besson</surname>
<given-names>Pascale</given-names>
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<xref ref-type="aff" rid="aff1">
<sup>1</sup>
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<aff id="aff1">
<sup>1</sup>
<institution>Universit&#xe9; Paris Cit&#xe9;, Institut de Physique du Globe de Paris</institution>, <addr-line>CNRS, Paris</addr-line>, <country>France</country>
</aff>
<aff id="aff2">
<sup>2</sup>
<institution>X-Ray Science Division, Advanced Photon Source, Argonne National Laboratory</institution>, <addr-line>Lemont, IL</addr-line>, <country>United States</country>
</aff>
<aff id="aff3">
<sup>3</sup>
<institution>Environmental Science Division, Argonne National Laboratory</institution>, <addr-line>Argonne, IL</addr-line>, <country>United States</country>
</aff>
<author-notes>
<fn fn-type="edited-by">
<p>Edited by: Cecile Guieu, UMR7093 Laboratoire d&#x2019;oc&#xe9;anographie de Villefranche (LOV), France</p>
</fn>
<fn fn-type="edited-by">
<p>Reviewed by: Kathrin Wuttig, University of Tasmania, Australia</p>
<p>Ashwini Kumar, Council of Scientific and Industrial Research (CSIR), India</p>
</fn>
<fn fn-type="corresp" id="fn001">
<p>*Correspondence: Cl&#xe9;ment Demasy, <email xlink:href="mailto:demasy@sun.ac.za">demasy@sun.ac.za</email>
</p>
</fn>
</author-notes>
<pub-date pub-type="epub">
<day>26</day>
<month>04</month>
<year>2024</year>
</pub-date>
<pub-date pub-type="collection">
<year>2024</year>
</pub-date>
<volume>11</volume>
<elocation-id>1363088</elocation-id>
<history>
<date date-type="received">
<day>29</day>
<month>12</month>
<year>2023</year>
</date>
<date date-type="accepted">
<day>12</day>
<month>04</month>
<year>2024</year>
</date>
</history>
<permissions>
<copyright-statement>Copyright &#xa9; 2024 Demasy, Boye, Lai, Burckel, Feng, Losno, Borensztajn and Besson</copyright-statement>
<copyright-year>2024</copyright-year>
<copyright-holder>Demasy, Boye, Lai, Burckel, Feng, Losno, Borensztajn and Besson</copyright-holder>
<license xlink:href="http://creativecommons.org/licenses/by/4.0/">
<p>This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) and the copyright owner(s) are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.</p>
</license>
</permissions>
<abstract>
<p>Although the input of desert dust as a key source of trace metals in the Southern Ocean (SO) has been previously studied, the dissolution process of metals in surface waters, particularly iron (Fe), remain poorly understood. Given the crucial role of Fe in primary production and the biological carbon pump in the SO, we focused on experimental estimations of Fe dissolution from Patagonian dust, the primary natural dust source in the SO. Our study considered both current and projected future conditions, encompassing sea-surface warming, acidification, increased photosynthetically active radiation, and doubled dust inputs. Through controlled laboratory experiments using filtered SO seawater, conducted over 7 days, we assessed changes in particulate Fe (pFe) concentrations, Fe redox speciation (Fe(II)/Fe(III)), and in the mineralogy of Fe-bearing dust in abiotic condition. The predominant minerals in the dust included quartz and aluminosilicates, with silicon (Si), aluminum (Al), and Fe as the major elements. No significant alterations in the mineralogy and the elemental composition of the dust were recorded during the dissolution experiments, neither under present nor under projected future conditions. The particulate Fe(II)/Fe(III) ratio remained consistently at 0.25 during the experiments, unaffected by changed conditions. Consequently, changes in environmental conditions in the SO would therefore not significantly alter the mineralogy and redox speciation of pFe in the Patagonian dust. On the contrary, pFe exhibited a dissolution rate of 3.8% and 1.6% per day under present and future conditions, respectively. The environmental changes anticipated for 2100 in the SO will likely to result in a decrease in the dissolution rate of pFe. Thus, even though a doubling of dust input by 2100 is anticipated, it will unlikely provide significantly more dissolved Fe (dFe) in seawater in the SO. Consequently, the future intensification of Patagonian dust inputs may not alleviate the Fe limitation in the SO.</p>
</abstract>
<kwd-group>
<kwd>Patagonian dust</kwd>
<kwd>iron</kwd>
<kwd>dissolution</kwd>
<kwd>Southern Ocean</kwd>
<kwd>anthropogenic changes</kwd>
</kwd-group>
<counts>
<fig-count count="7"/>
<table-count count="4"/>
<equation-count count="7"/>
<ref-count count="115"/>
<page-count count="18"/>
<word-count count="11474"/>
</counts>
<custom-meta-wrap>
<custom-meta>
<meta-name>section-in-acceptance</meta-name>
<meta-value>Ocean Observation</meta-value>
</custom-meta>
</custom-meta-wrap>
</article-meta>
</front>
<body>
<sec id="s1">
<title>Highlights</title>
<list list-type="bullet">
<list-item>
<p>The mineralogy of Patagonian dust was dominated by quartz and plagioclase, and the mineralogy of iron (Fe) was dominated by heterosite and Fe(III) sulfate hydrate. Fe(II) redox state was present at ~20% in the dust.</p>
</list-item>
<list-item>
<p>The mineralogy and redox speciation of particulate Fe in the dust remained stable during the 7-day dissolution experiments, unaffected by the present or future conditions (temperature, PAR, pH, dust concentration).</p>
</list-item>
<list-item>
<p>The Fe dissolution rate of Patagonian dust was 3.8% per day under present conditions and approximatively half of the rate (1.8% per day) under future conditions.</p>
</list-item>
<list-item>
<p>Even though a doubling of dust input by 2100 is anticipated, it will unlikely provide significantly more dissolved Fe in seawater in the Southern Ocean.</p>
</list-item>
</list>
</sec>
<sec id="s2" sec-type="intro">
<label>1</label>
<title>Introduction</title>
<p>Desertification linked to a decrease in precipitation is an emerging issue on Earth in the context of the climate change. Although since 1980, there has been no real trend of global increase in desert areas, Intergovernmental Panel on Climate Change (IPCC) projections for 2100 (RCP8.5) indicate a tendency to a 25% expansion of existing desert regions except for Antarctica (<xref ref-type="bibr" rid="B74">P&#xf6;rtner et&#xa0;al., 2022</xref>). Deserts are the major source of aerosols in the Earth&#x2019;s atmosphere compared to anthropogenic activities, fire and volcanic sources (<xref ref-type="bibr" rid="B76">Prospero et&#xa0;al., 2002</xref>; <xref ref-type="bibr" rid="B40">Hamilton et&#xa0;al., 2022</xref>). The desertic dusts are originated from the Earth&#x2019;s crust and they are dispersed across the atmosphere and the oceans via extensive air-mass circulations (<xref ref-type="bibr" rid="B56">Mahowald et&#xa0;al., 2005</xref>). These small particles (&lt; 10 &#xb5;m) mobilized by the winds have impacts on the climate and human health (<xref ref-type="bibr" rid="B38">Griffin and Kellogg, 2004</xref>; <xref ref-type="bibr" rid="B64">Miller et&#xa0;al., 2014</xref>). Upon settling on surface waters, these particles undergo dissolution, releasing crustal elements to the oceanic regions farthest from the continents. Thus, the dusts can provide macronutrients and nutritive metals such as iron (Fe), which are essential to the metabolism of microalgae (<xref ref-type="bibr" rid="B54">Lohan and Tagliabue, 2018</xref>). The phytoplankton, at the base of the biological carbon pump, indeed needs micro- and macro-nutrients to grow and capture carbon dioxide (CO<sub>2</sub>) via photosynthesis, while the synthetized organic carbon can be exported at depth (<xref ref-type="bibr" rid="B104">Tr&#xe9;guer et&#xa0;al., 2018</xref>). The storage of carbon on the seafloor allows to decrease the greenhouse effect in the atmosphere (<xref ref-type="bibr" rid="B82">Raven and Falkowski, 1999</xref>) and ensures a negative feedback on the climate change. Therefore, dusts have a pivotal role by supplying nutrients to phytoplankton, particularly in nutrient-limited oceanic regions.</p>
<p>In the Southern hemisphere, the Patagonian desert is the main source of dust to the Southern Ocean (SO), representing 58% of the total atmospheric deposit at these high latitudes (<xref ref-type="bibr" rid="B35">Gass&#xf3; and Stein, 2007</xref>; <xref ref-type="bibr" rid="B51">Li et&#xa0;al., 2008</xref>). Since the pre-industrial revolution, global dust deposition may have doubled, with projections in South America indicating an increasing contribution, partly driven by increased droughts and wind intensity (<xref ref-type="bibr" rid="B115">Zickfeld et&#xa0;al., 2007</xref>; <xref ref-type="bibr" rid="B57">Mahowald et&#xa0;al., 2010</xref>; <xref ref-type="bibr" rid="B36">Gass&#xf3; and Torres, 2019</xref>; <xref ref-type="bibr" rid="B74">P&#xf6;rtner et&#xa0;al., 2022</xref>). Patagonian dust is transported across the Atlantic and Indian sectors of the SO (<xref ref-type="bibr" rid="B51">Li et&#xa0;al., 2008</xref>). South of the Polar Front (&gt; 50&#xb0;S), surface waters are characterized as High Nutrient-Low Chlorophyll (HNLC), meaning that they are rich in macronutrients but primary production remains low. The deficit of Fe inputs significantly restricts the growth of phytoplankton in these waters (<xref ref-type="bibr" rid="B58">Martin, 1990</xref>), compounded by the low inputs of other micronutrients such as manganese (<xref ref-type="bibr" rid="B15">Browning et&#xa0;al., 2021</xref>). In this HNLC area, the low net primary production is proportional to the extremely low input of Fe that dissolves from the aerosols (<xref ref-type="bibr" rid="B17">Cassar et&#xa0;al., 2007</xref>). Furthermore, dust input into the SO has the potential to modify global climate by providing Fe and other essential limiting micronutrients, as evidenced by connections between increased dust inputs during Glacial periods and the emergence of the deep glaciations that characterize the past 1 Ma of Earth&#x2019;s history (<xref ref-type="bibr" rid="B59">Mart&#xed;nez-Garcia et&#xa0;al., 2011</xref>). In the context of the nowadays climate change, the intensification of Patagonian dust input therefore deserves heightened consideration. Understanding and anticipating the inputs of dissolved and bioavailable micronutrients by the Patagonian dust are critical to accurately project the evolution of the efficiency of the biological carbon pump in the future SO and its feedbacks on atmospheric CO<sub>2</sub>.</p>
<p>The mineralogy and redox speciation of dust-borne Fe could have played a major role in its bioavailability for the Southern ecosystem during glacial periods (<xref ref-type="bibr" rid="B94">Shoenfelt et&#xa0;al., 2018</xref>). The ability of Fe-oxides to release Fe into seawater is closely related with their crystalline structure (<xref ref-type="bibr" rid="B9">Bonneville et&#xa0;al., 2009</xref>; <xref ref-type="bibr" rid="B7">Bligh and Waite, 2011</xref>), the specific surface area (<xref ref-type="bibr" rid="B85">Roden, 2003</xref>) and the aggregation process (<xref ref-type="bibr" rid="B79">Raiswell, 2011</xref>). Thus, the nature of Fe in the dust can profoundly impact its dissolution rate in seawater, thereby influencing phytoplankton growth, productivity, and the overall functioning of the biological carbon pump in the SO (<xref ref-type="bibr" rid="B27">Deppeler and Davidson, 2017</xref>). Patagonian dust exhibits a distinct chemical composition, dominated by quartz, and crystallinity (grain size&lt;5 &#x3bc;m) (<xref ref-type="bibr" rid="B77">Qu, 2016</xref>) compared to other desertic dusts like those from Sahara, characterized by a relatively high presence of illite and a central size class typically ranging between 10-20 &#x3bc;m (<xref ref-type="bibr" rid="B66">Molinaroli, 1996</xref>; <xref ref-type="bibr" rid="B39">Guieu et&#xa0;al., 2002</xref>; <xref ref-type="bibr" rid="B50">Laity, 2008</xref>). Moreover, the SO, where these particles settle, also features specific physical (cold temperature, mixed layer depth of 50-90 m) and biogeochemical (HNLC area, dominance of diatoms south of the Polar Front) characteristics compared to other oceans (<xref ref-type="bibr" rid="B24">De Broyer et&#xa0;al., 2014</xref>). As a result, any alterations in the mineralogy and redox speciation of Patagonian Fe-dust in the future SO would be indicative of this region unique characteristics, but such variations have not been investigated yet.</p>
<p>While previous research has focused on the solubility and speciation of dust-borne elements under varying atmospheric pH conditions (<xref ref-type="bibr" rid="B91">Shi et&#xa0;al., 2012</xref>; <xref ref-type="bibr" rid="B40">Hamilton et&#xa0;al., 2022</xref>), relatively few studies have specifically investigated the behavior of aerosols in seawater (<xref ref-type="bibr" rid="B63">Meskhidze et&#xa0;al., 2019</xref>), with even fewer focusing on the speciation of Fe within dust particles (<xref ref-type="bibr" rid="B88">Schroth et&#xa0;al., 2009</xref>). For instance, it has been shown that Fe speciation in aerosols can differ depending on the aerosol source, with soils in arid regions dominated by Fe-oxides, glacial flour by primary and secondary ferrous silicates, and oil fly ash by ferric sulphate salts, corresponding, respectively, to Fe solubility of less than 1%, 2-3%, and 77-81% in the ocean (<xref ref-type="bibr" rid="B88">Schroth et&#xa0;al., 2009</xref>). To date, no comprehensive study focused on the Fe mineralogy and redox speciation in Patagonian dust. Additionally, only a very few studies have explored aerosol dissolution in seawater. Previous research predominantly simulated atmospheric conditions, incorporating diverse dust origins and experimental variables such as temperature, irradiation, and pH (<xref ref-type="bibr" rid="B91">Shi et&#xa0;al., 2012</xref>), illustrating the pivotal role of environmental factors in dust dissolution. In seawater, dissolution experiments were conducted using natural Cape Verde dust and anthropogenic aerosols to investigate the dissolution of cobalt (Co) and zinc (Zn) (<xref ref-type="bibr" rid="B100">Thur&#xf3;czy et&#xa0;al., 2010</xref>), as well as the Fe dissolution in Mediterranean waters using Saharan dust (<xref ref-type="bibr" rid="B109">Wagener et&#xa0;al., 2008</xref>). These studies revealed different dissolution rates of metals from dust in seawater, contingent on the dust source and quantity added, although only a subset of different dusts and trace elements were considered. Moreover, while a singular dissolution experiment involving Patagonian dust in seawater has been conducted, it primarily examined the dissolution of macronutrients (P, Si, N) (<xref ref-type="bibr" rid="B72">Paparazzo et&#xa0;al., 2018</xref>), indicating rapid dissolution upon contact with seawater. Given the key role that Patagonian dust can play in supplying Fe and supporting the biological carbon pump in the SO, it is essential to conduct new dissolution experiments considering the release of Fe.</p>
<p>To understand the processes of dissolution, it is imperative to investigate the mineralogical structure and redox speciation of the dust at the submicrometric scale. Synchrotron, owing to its power and precision, serves as an invaluable tool in investigating mineral physics. Previous synchrotron studies were performed on aerosols (<xref ref-type="bibr" rid="B70">Oakes et&#xa0;al., 2012</xref>; <xref ref-type="bibr" rid="B55">Longo et&#xa0;al., 2016</xref>) or marine particles (<xref ref-type="bibr" rid="B16">Campbell, 2013</xref>; <xref ref-type="bibr" rid="B44">Ingall et&#xa0;al., 2013</xref>; <xref ref-type="bibr" rid="B102">Toner et&#xa0;al., 2016</xref>). Atmospheric aerosols and marine particles revealed variations in mineralogical composition and Fe redox speciation typical of the origin and environmental processes undergone by the particle. In contrast, no study tracked the changes in Fe mineralogy and redox speciation during aerosol dissolution in seawater using synchrotron analyses.</p>
<p>In addition to the future intensification of dust deposition, the SO will experience other environmental changes, such as warming of 3&#xb0;C and acidification of -0.3 pH units of the surface waters, and increased photosynthetically active radiation (PAR) up to 55 &#x3bc;mol quanta m<sup>&#x2212;2</sup> s<sup>&#x2212;1</sup> (<xref ref-type="bibr" rid="B10">Boyd et&#xa0;al., 2016</xref>). Since these changes could have an impact on the dissolution of metals from dust, dissolution experiments simulating future SO conditions should also be considered (<xref ref-type="bibr" rid="B13">Breitbarth et&#xa0;al., 2010</xref>).</p>
<p>Therefore, this study aimed to assess the dissolution of pFe from Patagonian dust in seawater of the SO in the present and future environmental conditions. Particulate Fe dissolution was complemented by an analysis of associated processes within particulate Patagonian dust, including alterations in mineralogy, elemental composition, and Fe redox speciation. Controlled dissolution experiments were performed simulating the current and future-2100 conditions in terms of the key-selected variables (dust input, temperature, pH, PAR) over a period of one week. Dissolution rates were quantified based on the measurement of pFe using ICP-QMS, enabling estimation of the proportion of Fe released from the particulate phase. The underlying dissolution processes were investigated at the scales of the dust bulk (XRD analyses) and the single particle (synchrotron analyses). This approach allowed a detailed understanding of how the mineralogical composition and redox speciation of pFe were impacted by future conditions, and how they can affect dissolution processes. A significant contribution of this study was its pioneering estimate of Fe released by Patagonian dust, in addition to elucidating the nature of pFe over time, including mineralogical composition and redox speciation. This study provided the first estimations of the concentrations of Fe released by Patagonian dust, which may be readily available to phytoplankton in the present and future SO.</p>
</sec>
<sec id="s3" sec-type="materials|methods">
<label>2</label>
<title>Material and methods</title>
<sec id="s3_1">
<label>2.1</label>
<title>Production of Patagonian dust</title>
<p>The dust was generated from a Patagonian soil sampled in December 2011 at Lago Argentino at 50.29&#xb0;S-71.81&#xb0;W. This soil has an average elemental composition consistent with other areas of Patagonia (<xref ref-type="bibr" rid="B77">Qu, 2016</xref>), and represents one of the two primary reported dust sources in Patagonia (at 48.65&#xb0;S-69&#xb0;W and 50.6&#xb0;S-70&#xb0;W; <xref ref-type="bibr" rid="B35">Gass&#xf3; and Stein, 2007</xref>). Therefore, Patagonian dust generated from this soil is a representative proxy of dust emission from South America and deposited in the SO. A quantity of 200 g of soil was sampled from the 0-2 cm surface layer and stored in polyethylene bags. Then, the soil was sifted using a 0.84 mm sieve (<xref ref-type="bibr" rid="B77">Qu, 2016</xref>). In the laboratory, the SyGavib system (aerosol generation system by vibration) developed by (<xref ref-type="bibr" rid="B78">Qu et&#xa0;al., 2020</xref>) was employed to generate the dust from this sieved soil. This system employs a loudspeaker to induce vibrations and an air-pump system to facilitate the upward movement of the generated aerosols, mimicking natural wind processes. According to Stokes law, particles smaller than 10 &#xb5;m were transported to the top of the&#xa0;cylinder. Notably, atmospheric dust emitted from deserts consists of particles below 10 &#xb5;m, with the major fraction lower than 5 &#xb5;m (<xref ref-type="bibr" rid="B95">Sow et&#xa0;al., 2009</xref>). The system generates a bimodal aerosol distribution centered around 2-5 &#xb5;m and 0.3-0.5 &#xb5;m, corresponding to the distribution observed by <xref ref-type="bibr" rid="B95">Sow et&#xa0;al. (2009)</xref>. The generated aerosol was then collected onto a cleaned Polyethersulfone (PES) filter (0.2 &#xb5;m pore size from Supor<sup>&#xae;</sup>). Then, suprapur methanol was used to extract dust from the filter, rather than distilled water in order to prevent initiating the dissolution phase with acidic distilled water (pH ~5.8) and the formation of aggregates of dust particles. Furthermore, Patagonian dust from steppes contain a very low concentration of organic matter (&lt; 1%) (<xref ref-type="bibr" rid="B37">Gonz&#xe1;lez Polo et&#xa0;al., 2015</xref>), enabling the use of methanol without altering the dust composition. Dust generated was then gently crushed with an agate mortar to eliminate any large particles, thereby preventing sedimentation during the experiment.</p>
</sec>
<sec id="s3_2">
<label>2.2</label>
<title>Sampling of the seawater</title>
<p>The seawater used for the dissolution experiments was sampled from the High-Nutrient Low-Chlorophyll area in the Indian sector of the SO at 56.50&#xb0;S-63.00&#xb0;E in January 2020 aboard the French <italic>R.V. Marion Dufresne II</italic> from the surface (approx. 15 m depth) using a clean Teflon diaphragm pump with a flow rate of 15 L min<sup>-1</sup> and a 30 m PTFE pipe following ultra-clean trace metal clean sampling procedures (<xref ref-type="bibr" rid="B22">Cutter et&#xa0;al., 2017</xref>). Seawater flowed directly from the pipe under a laminar flow fume hood (HEPA 14 filter) in the vessel&#x2019;s laboratory. The seawater was filtered on-line using a cellulose acetate filter capsule (Sartorius<sup>&#xae;</sup>) featuring an inlet porosity of 0.45 &#xb5;m and an outlet porosity of 0.2 &#xb5;m. The filtered seawater was subsequently stored in 10 and 20 L acid cleaned polycarbonate (PC) containers (Nalgene<sup>&#xae;</sup>) at room temperature (21&#xb0;C) and in the dark. These incubation bottles underwent 48 h in DECON (2.5%), 1 week in HCl (10%) and filled with 2% distilled HCl until use.</p>
</sec>
<sec id="s3_3">
<label>2.3</label>
<title>Incubation of dust in seawater: set-up of the experimental conditions</title>
<p>To simulate the surface water conditions of the SO, temperature and light (<xref ref-type="table" rid="T1">
<bold>Table&#xa0;1</bold>
</xref>) were regulated using a thermostatic cabinet (Aqualytic<sup>&#xae;</sup>) fitted with light emitting diodes (LED) covered by a 201 full convert tungsten blue (CTB) filter (Lee filter<sup>&#xae;</sup>). The artificial light diffusion was set-up according to a daytime cycle from 4:00 am to 8:00 pm for the light and from 8:00 pm to 4:00 am for the night, resulting in a total light exposure of 16 h per day. Photosynthetic Active Radiation (PAR) was monitored in the incubator using a sensor MODEL MQ-510 Apogee<sup>&#xae;</sup> instruments placed in a PC bottle filled with Milli-Q water. The PAR was set at ~30 &#xb5;mol quanta m<sup>-</sup>&#xb2; s<sup>-1</sup> in the present conditions, and at ~55 &#xb5;mol quanta m<sup>-</sup>&#xb2; in the future conditions. Adjustment of PAR was achieved by the number of lit LEDs.</p>
<table-wrap id="T1" position="float">
<label>Table&#xa0;1</label>
<caption>
<p>Experimental conditions of the dissolution experiments representing the present and future surface waters in the SO.</p>
</caption>
<table frame="hsides">
<thead>
<tr>
<th valign="top" align="left"/>
<th valign="top" align="left">Present conditions</th>
<th valign="top" align="left">Future (2100) conditions</th>
</tr>
</thead>
<tbody>
<tr>
<td valign="top" align="left">Patagonian dust concentration (mg L<sup>-1</sup>)</td>
<td valign="top" align="left">1</td>
<td valign="top" align="left">2</td>
</tr>
<tr>
<td valign="top" align="left">pH</td>
<td valign="top" align="left">8.10</td>
<td valign="top" align="left">7.80</td>
</tr>
<tr>
<td valign="top" align="left">Temperature (&#xb0;C)</td>
<td valign="top" align="left">10.6</td>
<td valign="top" align="left">13.7</td>
</tr>
<tr>
<td valign="top" align="left">PAR (&#xb5;mol quanta m<sup>-2</sup> s<sup>-1</sup>)</td>
<td valign="top" align="left">30</td>
<td valign="top" align="left">55</td>
</tr>
</tbody>
</table>
<table-wrap-foot>
<fn>
<p>The selection of future pH, temperature, and PAR conditions was based on IPCC projections (RCP8.5) (<xref ref-type="bibr" rid="B10">Boyd et&#xa0;al., 2016</xref>; <xref ref-type="bibr" rid="B74">P&#xf6;rtner et&#xa0;al., 2022</xref>). Current Patagonian dust concentrations were estimated from (<xref ref-type="bibr" rid="B51">Li et&#xa0;al., 2008</xref>; <xref ref-type="bibr" rid="B43">Heimburger et&#xa0;al., 2013b</xref>). The doubling of dust input in the future was determined based on the anticipated evolution of atmospheric deposition patterns (<xref ref-type="bibr" rid="B35">Gass&#xf3; and Stein, 2007</xref>; <xref ref-type="bibr" rid="B57">Mahowald et&#xa0;al., 2010</xref>; <xref ref-type="bibr" rid="B92">Shi et&#xa0;al., 2023</xref>).</p>
</fn>
</table-wrap-foot>
</table-wrap>
<p>The pH conditions were regulated by gas exchange from saturation of the overhanging atmosphere of the seawater bottle with CO<sub>2</sub> mixture. This approach was specifically designed to emulate the natural acidification of the ocean, without causing any disruption to the carbonate system or altering the alkalinity (<xref ref-type="bibr" rid="B84">Riebesell et&#xa0;al., 2011</xref>). To initiate the experiments, the air space of the 10 L bottles containing seawater were saturated with pure CO<sub>2</sub> (Alphagas 1 purity<sup>&#xae;</sup>) for 1 min. Subsequently, the bottles were placed on a 3D rotating plate in order to stir the water and enhance the exchange between the air and the water for 15 min. A gas mixture containing 800 ppm of CO<sub>2</sub> (Alphagas 1 purity<sup>&#xae;</sup>) was then injected into the bottle air space until the target pH value of 7.80, representing the future conditions, was reached. Continuous pH monitoring was carried out throughout the experiment, and additional injections of the 800 ppm CO<sub>2</sub> gas mixture were made to adjust the pH if necessary.</p>
<p>Dry dust deposition was chosen over wet deposition for its prevalence in atmospheric inputs from South America (<xref ref-type="bibr" rid="B51">Li et&#xa0;al., 2008</xref>), and in order to mimic the anticipated intensification of winds and aridity, which are expected to increase dry deposition (<xref ref-type="bibr" rid="B74">P&#xf6;rtner et&#xa0;al., 2022</xref>). The mass of dust addition was deliberately overestimated by 1 mg L<sup>-1</sup>, exceeding a concentration of 9 ng L<sup>-1</sup> d<sup>-1</sup> or 282 ng L<sup>-1</sup> m<sup>-1</sup>, as measured in the deposition around Kerguelen Island (<xref ref-type="bibr" rid="B42">Heimburger et&#xa0;al., 2012</xref>). This overestimation was necessary to ensure accurate measurement of the dust&#x2019;s weight and to be able to detect the change in pFe concentration over the dissolution. Moreover, a lower mass can increase the heterogeneity in the composition of the inoculated dusts. A microbalance (Mettler Toledo MX5<sup>&#xae;</sup>), periodically calibrated, was used to weigh 10 mg and 20 mg of the dust. This resulted in a final concentration in the medium equivalent to 1 mg L<sup>-1</sup> in the present conditions and to 2&#xa0;mg L<sup>-1</sup> in the future conditions. Prior to the addition to seawater, the dust was mixed in a small volume of filtered seawater in an ultra-clean tube, which was placed on a vortex (vortex genie 2 Scientific Industries<sup>&#xae;</sup>) to ensure effective homogenization. Then, the dust-enriched solution was transferred to a final volume of 10 L of filtered seawater. These large volume bottles were vigorously agitated after the dust enrichment and then transferred to an incubator to set the physical conditions.</p>
<p>Throughout the incubation, a set of physico-chemical parameters was sampled upon dust addition (<xref ref-type="supplementary-material" rid="SM1">
<bold>Supplementary Information, Table&#xa0;1</bold>
</xref>), at the exact time of dust addition, then every 15 minutes during the first hour, every 30 minutes during the second hour, and subsequently every 24 hours over 7 days. This detailed monitoring approach aimed to capture any rapid dissolution processes that might occur during the initial contact of the dust with seawater (<xref ref-type="bibr" rid="B109">Wagener et&#xa0;al., 2008</xref>).</p>
</sec>
<sec id="s3_4">
<label>2.4</label>
<title>Observation using scanning electronic microscopy (SEM)</title>
<p>A 100 ml volume of seawater was filtered using a PC filter holder (Nalgene<sup>&#xae;</sup>) with a PC filter (porosity of 0.2 &#xb5;m, diameter of 47 mm, Nuclepore&#x2122;). The filters were then dried and stored in the dark at room temperature. Prior to microscopic examination, the filters underwent gold metallization. Observations of the dust during the dissolution experiments were conducted using a high-resolution focused ion beam-scanning electron microscope (FEG-FIB-SEM) Auriga 40 from Zeiss<sup>&#xae;</sup>, fitted with a Zeiss Gemini column (<xref ref-type="bibr" rid="B53">Liu et&#xa0;al., 2016</xref>). The instrument provides sub-nanometer scale resolution for detailed analysis of the dust particles.</p>
</sec>
<sec id="s3_5">
<label>2.5</label>
<title>Analyses of particulate trace metals</title>
<p>The novelty of this study was to monitor the dissolution of Fe by monitoring pFe. The particulate fraction is defined as the size fraction greater than 0.2 &#x3bc;m. Particulate trace metals were analyzed on ultra-clean Supor<sup>&#xae;</sup> PES filters (0.2 &#xb5;m, 47 mm) after filtration of 250 mL of seawater sample using PC filter holders (Nalgene<sup>&#xae;</sup>), previously cleaned using trace metal clean procedure (<xref ref-type="bibr" rid="B73">Planquette and Sherrell, 2012</xref>). The filter holder was connected to a clean air pump (0.5 L min<sup>-1</sup>), enabling rapid filtration of 1 L of sample within a few minutes. All these manipulations were carried out within a laminar flow fume hood in a clean room (ISO 5). Following filtration, the filters were carefully placed in ultra-clean petri dishes, and then dried under the laminar fume hood. The petri dishes were wrapped with parafilm and stored at -20&#xb0;C until analyses.</p>
<p>The digestion of the filter was performed in perfluoroalkoxy alkanes (PFA) vials (Savillex<sup>&#xae;</sup>) using the method adapted from <xref ref-type="bibr" rid="B73">Planquette and Sherrell (2012)</xref>. The filter was positioned on the inner wall of the vial to prevent the complete digestion of the filter by soaking it directly in acid. A 3 mL solution of 8.0 M distilled HNO<sub>3</sub>
<sup>-</sup>/2.9 M distilled HF was poured at the bottom of the vial and the solution was left to reflux overnight at 130&#xb0;C on a PFA coating hot plate inside a controlled atmosphere evaporation station (Elemental Scientific<sup>&#xae;</sup>). After cooling, the vial was opened, and the filter was carefully removed from the vial wall. The acid was evaporated at 110&#xb0;C until complete dryness. Subsequently, the residue was remobilized in 1 mL of a 50% distilled HNO<sub>3</sub>
<sup>-</sup> solution at 70&#xb0;C for over an hour. Once cooled, 14 mL of MQ water was added to the solution, resulting in a homogenized solution of particulate trace metals for Fe analysis using inductively coupled plasma quadrupole mass spectrometry (ICP-QMS).</p>
<p>Elemental concentrations were assessed using an Agilent 7900 quadrupole ICP-MS. Fe and Al were measured using a collision-reaction cell with helium gas (5 mL min<sup>-1</sup>) to remove polyatomic interferences. A scandium internal-standard was injected after inline mixing with the samples to correct for signal drift and matrix effects. A set of multi-element calibration standards was analyzed to confirm and model (through simple linear regression) the linear relationship between signal and concentration. The model was then used to convert measured sample counts to concentrations. Reported uncertainties were calculated using error propagation equations and considering the combination of standard deviation on consecutive signal integrations (n = 3), internal-standard ratio and blank subtraction. The non-linear term (internal-standard ratio) was linearized using a first-order Taylor series expansion to simplify error propagation.</p>
<p>Three measurement sessions on different days were necessary to measure all samples presented in this study. Across these three sessions, the background equivalent concentrations (BEC) of the ICP-MS was below 0.5 ppb for both Al and Fe. Chemistry blanks averaged at 0.15 &#xb1; 0.1 ppb (1SD) and 3.2 &#xb1; 2 ppb (1SD). These values are well below the lowest concentrations of the samples measured, which were above 400 ppb for both Al and Fe. The impact of the BEC and contaminations on our experiments is therefore neglectable. Repeatability was assessed both within a measurement session and across the different sessions, by measuring some standards, dry dust sample (PB1) and Hawaiian Volcano Observatory Basalt (BHVO1), (<xref ref-type="supplementary-material" rid="SM1">
<bold>Supplementary Information, Table&#xa0;2</bold>
</xref>) twice within a session (beginning and end) and across sessions. It is calculated as the standard deviation of repeated measurements divided by the mean and expressed in percent. Repeatability results are good as we observe less than 2.5% variability (1SD) within a session and less than 3.5% variability (1SD) across sessions for both Al and Fe. Finally, accuracy was assessed by estimating the deviation of the concentration of the two solid standards from their reference values. It is found to be of -5.1% and 9.8% for Al and -8.9% and 12.8% for Fe, in standards PB1 and BHVO1 respectively. These results are acceptable and can be explained by the relative standard deviation of the measured concentrations of digestion replicates which is between 10% and 15%. These standard deviations are likely related to the accuracy of the scale and the potential loss of material while weighing 1 mg of standards. The absence of systematic accuracy offset further comforts us in the quality of the calibration model. As the experiment could not be replicated, the uncertainty was calculated based on repeated measurements from the ICP-QMS.</p>
</sec>
<sec id="s3_6">
<label>2.6</label>
<title>X-Ray diffraction analyses</title>
<p>The X-ray diffraction (XRD) analysis method was employed to identify mineral phases, crystal sizes, and morphologies. The detection was performed using a diffractometer (PANALYTICAL X&#x2019;PERT PRO) fitted with a Co tube and a X&#x2019;celerator detector. The analyses were done with the Patagonian soil and dust that were polycrystalline powder, characterized by a condensed and ordered state with fine granulometry, ensuring accurate analysis with wider peaks. The powder was deposited onto a steel sample holder and brushed to create a flat surface for analyses. The data acquisition was repeated 3 times and required 20 minutes to prevent detector saturation and a subsequent decrease in peak intensities. The diffracted ray was captured using a PIXcel 3D detector (Panalytical<sup>&#xae;</sup>), converting the photons into an electrical signal. The HighScore Plus (HS+) software was used to compute the mean curve from the three repeated diffractograms. Each peak position in the diffractogram corresponded to a specific element, and the peak intensity was directly proportional to its relative abundance. A comparison of the peaks with the mineralogical reference database &#x201c;ICSD FIZ Karlsruhe2&#x201d; enabled the identification of each mineral present in the sample based on its chemical composition and crystallographic structure. Quantitative analyses were performed by comparing the peak areas of the different minerals. This estimation was conducted using the Rietveld method in conjunction with the HighScore Plus (HS+) software (<xref ref-type="bibr" rid="B19">Chung, 1974</xref>; <xref ref-type="bibr" rid="B69">Nowak et&#xa0;al., 2018</xref>).</p>
</sec>
<sec id="s3_7">
<label>2.7</label>
<title>Synchrotron analyses</title>
<p>Another original objective of this study was to investigate the implication of mineralogy and speciation redox of pFe to Fe dissolution using synchrotron analysis. At different incubation times, 500 ml of seawater samples were filtered onto PC filters Nuclepore&#x2122; (pore size of 0.2 &#xb5;m, diameter of 47 mm), using PC filter holders (Nalgene<sup>&#xae;</sup>). The filters were placed in a petri dish and dried under a fume hood. To prevent any oxidation processes, the samples were stored in a desiccator under a nitrogen atmosphere and shielded from light using 280 black foil (Lee filters<sup>&#xae;</sup>). For the analytical procedures, a section of the filter was selected and cut using ethanol-cleaned tweezers and scissors. The selection of the zone to be cut was guided by a brief observation under an optical microscope to identify regions with the presence of particles. The cut section was smaller than 1 cm<sup>2</sup>. The piece was then positioned on one of the 2 slots of an aluminium (Al) sample stick. During the analysis, the samples were positioned in a helium-filled chamber to limit the absorption of the fluorescence signal by the oxygen molecules. The analyses were performed at the Chicago synchrotron, APS (Advanced Photon Source) on the Beamline 2-ID-D. The detector used was a silicon drift detector (Vortex EM), with a sensitivity area of 50-mm&#xb2; and a Be 12.5-mm window SII (NanoTechnology, Northridge CA, USA). Two types of analyses were performed on this sector, micro-fluorescence and micro-XANES analyses (<xref ref-type="bibr" rid="B61">McNulty et&#xa0;al., 2003</xref>).</p>
<p>For all micro-fluorescence analyses (micro-XRF), the dwell time was set at 100 ms, and the step size was defined as 0.25 &#xb5;m. The coarse mode analysis utilized a spot size of 100 x 100 &#xb5;m, which represented approximately 0.0006% of the total air filter. Based on the coarse scan, the size and location of the spot for the fine scans (56 x 56 &#xb5;m, equivalent to 0.0002% of total air filter) were selected. Two spots of analysis were then acquired per sample. The X-ray was fixed at 7200 eV to enable the collection of elements from Al to Fe, which included Al, silicon (Si), phosphorus (P), sulfur (S), chlorine (Cl), potassium (K), calcium (Ca), titanium (Ti), vanadium (V), chromium (Cr), manganese (Mn), and Fe. In this study, the target elements were Fe, Al, and Si. To ensure accurate calibration of the elemental scans, NBS 1832 and 1833 thin film standards from the National Bureau of Standards (Gaithersburg, MD) were employed. These standards provide known values for each element in terms of weight percentage (% by wt) and X-ray absorption peak (k&#x3b1; and k&#x3b2;). Quantification of the samples was achieved through proportionality to the certified standard of known percentage by wt. Then, the average value of density by areas (&#xb5;g cm<sup>-</sup>&#xb2;) was calculated according to <xref ref-type="disp-formula" rid="eq1">Equation 1</xref>.</p>
<disp-formula id="eq1">
<label>(1)</label>
<mml:math display="block" id="M1">
<mml:mrow>
<mml:mtext>Average&#xa0;density&#xa0;by&#xa0;areas&#xa0;</mml:mtext>
<mml:mrow>
<mml:mo stretchy="false">(</mml:mo>
<mml:mrow>
<mml:mi>&#xb5;</mml:mi>
<mml:mtext>g</mml:mtext>
<mml:mi>&#xa0;</mml:mi>
<mml:msup>
<mml:mtext>cm</mml:mtext>
<mml:mrow>
<mml:mo>-</mml:mo>
<mml:mn>2</mml:mn>
</mml:mrow>
</mml:msup>
</mml:mrow>
<mml:mo stretchy="false">)</mml:mo>
</mml:mrow>
<mml:mo>=</mml:mo>
<mml:mfrac>
<mml:mrow>
<mml:mrow>
<mml:mo stretchy="false">(</mml:mo>
<mml:mrow>
<mml:mo>%</mml:mo>
<mml:mtext>&#xa0;by&#xa0;wt</mml:mtext>
</mml:mrow>
<mml:mo stretchy="false">)</mml:mo>
</mml:mrow>
<mml:mo>&#xd7;</mml:mo>
<mml:mtext>&#xa0;</mml:mtext>
<mml:msup>
<mml:mn>10</mml:mn>
<mml:mrow><mml:mo>-</mml:mo>
<mml:mn>2</mml:mn></mml:mrow>
</mml:msup>
<mml:mo>&#xd7;</mml:mo>
<mml:mtext>film&#xa0;wt&#xa0;</mml:mtext>
<mml:mrow>
<mml:mo stretchy="false">(</mml:mo>
<mml:mrow>
<mml:mi>&#xb5;</mml:mi>
<mml:mtext>g</mml:mtext>
</mml:mrow>
<mml:mo stretchy="false">)</mml:mo>
</mml:mrow>
</mml:mrow>
<mml:mrow>
<mml:mn>10.06</mml:mn>
<mml:mtext>&#xa0;</mml:mtext>
<mml:mrow>
<mml:mo stretchy="false">(</mml:mo>
<mml:mrow>
<mml:msup>
<mml:mtext>cm</mml:mtext>
<mml:mn>2</mml:mn>
</mml:msup>
</mml:mrow>
<mml:mo stretchy="false">)</mml:mo>
</mml:mrow>
</mml:mrow>
</mml:mfrac>
</mml:mrow>
</mml:math>
</disp-formula>
<p>The uncertainty in the film mass (film wt in <xref ref-type="disp-formula" rid="eq1">Equation 1</xref>) and area (10.06 cm<sup>2</sup>) was negligible compared to the estimated uncertainty in the certified values and thus, it can be neglected in the <xref ref-type="disp-formula" rid="eq1">Equation 1</xref>. Data processing was carried out using the IDL MAPS software (<xref ref-type="bibr" rid="B107">Vogt, 2003</xref>), which converts the data into &#xb5;g cm<sup>-</sup>&#xb2; of micro-fluorescence scans. These results enabled to characterize the metal concentration according to the filter surface, along with the ratios between the elements. Areas identified by the software with high metal concentrations were designated as individual particles. This approach facilitated the calculation of elemental concentrations per particle at a microscopic scale. With the assistance of the software, a plot of the particle area was generated, and mean element concentrations were extracted per pixel (0.062 &#xb5;m&#xb2;).</p>
<p>Micro-XANES (X-ray Absorption Near Edge Structure) provides valuable insights into the oxidation state of the element studied. The oxidation state was effectively determined by the position of the pre-edge centroid, as opposed to the K-edge centroid, due to the reduced impact of matrix effects at this specific peak (<xref ref-type="bibr" rid="B3">Bajt et&#xa0;al., 1994</xref>). The XANES analysis was measured with a 250 &#xb5;m beam. The zone plate used was 150 &#xb5;m in diameter, and the focal length was 64 mm at 7.18 eV, corresponding to the Fe peak. Given the relatively high concentrations of dust added in our experiments compared to the ambient seawater, the signal intensities were well above the detection limits. To determine the oxidation state, the pre-edge centroid was initially normalized by subtracting the background of the absorption peak of the pre-edge, resulting in a Gaussian curve. The position of the peak of this Gaussian curve was then utilized in <xref ref-type="disp-formula" rid="eq2">Equation 2</xref> for converting the position of the K-edge XANES centroid spectrum of Fe(II) mineral to % oxidation state (<xref ref-type="bibr" rid="B70">Oakes et&#xa0;al., 2012</xref>).</p>
<disp-formula id="eq2">
<label>(2)</label>
<mml:math display="block" id="M2">
<mml:mrow>
<mml:mo>%</mml:mo>
<mml:mtext>&#xa0;</mml:mtext>
<mml:mi mathvariant="normal">F</mml:mi>
<mml:mi mathvariant="normal">e</mml:mi>
<mml:mrow>
<mml:mo stretchy="false">(</mml:mo>
<mml:mrow>
<mml:mi mathvariant="normal">I</mml:mi>
<mml:mi mathvariant="normal">I</mml:mi>
</mml:mrow>
<mml:mo stretchy="false">)</mml:mo>
</mml:mrow>
<mml:mo>=</mml:mo>
<mml:mn>100</mml:mn>
<mml:mo>&#x2212;</mml:mo>
<mml:mfrac>
<mml:mrow>
<mml:mi>C</mml:mi>
<mml:mi>e</mml:mi>
<mml:mi>n</mml:mi>
<mml:mi>t</mml:mi>
<mml:mi>r</mml:mi>
<mml:mi>o</mml:mi>
<mml:mi>i</mml:mi>
<mml:mi>d</mml:mi>
<mml:mo>&#xa0;</mml:mo>
<mml:mi>p</mml:mi>
<mml:mi>o</mml:mi>
<mml:mi>s</mml:mi>
<mml:mi>i</mml:mi>
<mml:mi>t</mml:mi>
<mml:mi>i</mml:mi>
<mml:mi>o</mml:mi>
<mml:mi>n</mml:mi>
<mml:mo>&#x2212;</mml:mo>
<mml:mn>7.1129</mml:mn>
</mml:mrow>
<mml:mrow>
<mml:mn>0.0143</mml:mn>
</mml:mrow>
</mml:mfrac>
</mml:mrow>
</mml:math>
</disp-formula>
<p>To discern the nature of the Fe compounds present in the Patagonian dust, our analysis involved a comprehensive comparison of the samples using the data of Fe mineral powders (26 Fe mineral standards) provided by <xref ref-type="bibr" rid="B70">Oakes et&#xa0;al. (2012)</xref>. The characterization of Fe minerals from the XANES spectra was achieved through a combination linear fitting using the Athena software (<xref ref-type="bibr" rid="B81">Ravel and Newville, 2005</xref>). It is important to note that each sample was subjected to dual micro-XANES and micro-XRF analyses, targeting different spots within the filters. Therefore, the uncertainty was determined using the standard deviation based on two measurements from two distinct spots on the same filter. This approach ensured a robust and reliable assessment of the Fe compounds, contributing to a more comprehensive understanding of the oxidation state and mineralogical composition of the Patagonian dust.</p>
</sec>
</sec>
<sec id="s4" sec-type="results">
<label>3</label>
<title>Results and discussion</title>
<sec id="s4_1">
<label>3.1</label>
<title>Composition, mineralogy and Fe redox speciation of the Patagonian dust</title>
<p>The elemental composition, the size and the crystallinity of the dust can significantly influence the process of Fe dissolution in seawater (<xref ref-type="bibr" rid="B2">Anbeek, 1992</xref>; <xref ref-type="bibr" rid="B86">Rubasinghege et&#xa0;al., 2010</xref>). Notably, research has demonstrated that despite the specific surface area, Fe from clays exhibits higher solubility (4%) compared to Fe-oxides (&lt; 1%) (<xref ref-type="bibr" rid="B47">Journet et&#xa0;al., 2008</xref>; <xref ref-type="bibr" rid="B45">Ito et&#xa0;al., 2021</xref>). In our study, X-ray Diffraction (XRD) analyses were conducted on Patagonian soil and dry dust to characterize the dust mineralogy. Our results indicated the prevalence of framework silicates in both the soil and dust (<xref ref-type="table" rid="T2">
<bold>Table&#xa0;2</bold>
</xref>), commonly found across Patagonia (<xref ref-type="bibr" rid="B30">Desiage et&#xa0;al., 2018</xref>). This family of minerals is the most widespread in the Earth&#x2019;s upper crust as well as in desertic soils, including quartz (SiO<sub>2</sub>) and plagioclases (albite NaAlSi<sub>3</sub>O<sub>8</sub> or anorthite CaAl<sub>2</sub>Si<sub>2</sub>O<sub>8</sub>), alongside sheet silicates such as muscovite (KAl<sub>2</sub>(AlSi<sub>3</sub>O<sub>10</sub>)) and tectosilicate with barrerite ((Na,K,Ca)<sub>2</sub> Al<sub>2</sub> Si<sub>7</sub> O<sub>18</sub> 7H<sub>2</sub>O) (<xref ref-type="bibr" rid="B68">Nesse, 2017</xref>). XRD analysis revealed that all identified minerals within the dust exhibited ordered distributions, suggesting relatively low susceptibility to dissolution (<xref ref-type="bibr" rid="B80">Ramseyer et&#xa0;al., 1992</xref>). Similar mineralogy were found between Patagonian soil and dust, as previously observed by <xref ref-type="bibr" rid="B77">Qu (2016)</xref>, indicating that the production of dust from soil preserved the mineralogical diversity. However, the notable change between soil and dust was a loss of plagioclases (<xref ref-type="table" rid="T2">
<bold>Table&#xa0;2</bold>
</xref>). Moreover, these measurements, while informative, were unable to capture the presence of amorphous compounds that possess higher dissolution capacity.</p>
<table-wrap id="T2" position="float">
<label>Table&#xa0;2</label>
<caption>
<p>X-ray Diffraction (XRD) analyses of Patagonian soil and dry dust (this study) and of surface sediments of the Gulf of San Jorge (<xref ref-type="bibr" rid="B30">Desiage et&#xa0;al., 2018</xref>).</p>
</caption>
<table frame="hsides">
<thead>
<tr>
<th valign="top" align="center">Mineral composition (%)</th>
<th valign="top" align="center">Patagonian soil<break/>(this study)</th>
<th valign="top" align="center">Dry Patagonian dust<break/>(this study)</th>
<th valign="top" align="center">Surface sediment in the Gulf of San Jorge central Patagonia (<xref ref-type="bibr" rid="B30">Desiage et&#xa0;al., 2018</xref>)</th>
</tr>
</thead>
<tbody>
<tr>
<td valign="middle" align="left">Quartz</td>
<td valign="middle" align="center">29.1</td>
<td valign="middle" align="center">50.7</td>
<td valign="top" align="center">14-51</td>
</tr>
<tr>
<td valign="middle" align="left">Plagioclase</td>
<td valign="middle" align="center">62.1</td>
<td valign="middle" align="center">37.7</td>
<td valign="top" align="center">15-49</td>
</tr>
<tr>
<td valign="middle" align="left">Muscovite</td>
<td valign="middle" align="center">8.1</td>
<td valign="middle" align="center">9.9</td>
<td valign="top" align="center"/>
</tr>
<tr>
<td valign="middle" align="left">Barrerite</td>
<td valign="middle" align="center">0.6</td>
<td valign="middle" align="center">1.7</td>
<td valign="top" align="center"/>
</tr>
<tr>
<td valign="middle" align="left">Clays</td>
<td valign="middle" align="center"/>
<td valign="middle" align="center"/>
<td valign="top" align="center">2-41</td>
</tr>
<tr>
<td valign="middle" align="left">Amorphous silica</td>
<td valign="middle" align="center"/>
<td valign="middle" align="center"/>
<td valign="top" align="center">4.5-35.5</td>
</tr>
<tr>
<td valign="middle" align="left">K-feldspar</td>
<td valign="middle" align="center"/>
<td valign="middle" align="center"/>
<td valign="top" align="center">2-12</td>
</tr>
</tbody>
</table>
</table-wrap>
<p>The composition of Patagonian dust revealed 7.1% of Al, and 3.9% of Fe, respectively. Furthermore, this finding reinforced the notion that Al and Fe were the dominant metals within the Patagonian dust, as supported by XRD analyses (<xref ref-type="table" rid="T3">
<bold>Table&#xa0;3</bold>
</xref>). The&#xa0;similar composition of the Patagonian dust used in this study and the average composition of the Earth&#x2019;s crust (<xref ref-type="bibr" rid="B111">Wedepohl, 1995</xref>) suggested that the dust was representative of a desert aerosol. Notably, desert dusts are typically characterized as weathered materials, having undergone the effects of aging, and they are comparatively more resistant to dissolution compared to anthropogenic dust (<xref ref-type="bibr" rid="B29">Desboeufs et&#xa0;al., 2005</xref>). Elemental composition analyses of the dust also displayed values ranging in the same records as for river and aeolian samples from Patagonia (<xref ref-type="table" rid="T3">
<bold>Table&#xa0;3</bold>
</xref>; <xref ref-type="bibr" rid="B34">Gaiero et&#xa0;al., 2003</xref>). Furthermore, while Fe was one of the most abundant element in the samples, it was not directly associated with these Si-minerals (<xref ref-type="table" rid="T2">
<bold>Table&#xa0;2</bold>
</xref>). Notably, in natural dust, Fe-oxide minerals can be difficult to discern among clay minerals (<xref ref-type="bibr" rid="B49">Koffman et&#xa0;al., 2021</xref>), because amorphous Fe forms remain undetectable by XRD.</p>
<table-wrap id="T3" position="float">
<label>Table&#xa0;3</label>
<caption>
<p>Element concentrations in Patagonian dust measured in this study, in Patagonian riverborne and windborne samples, and the average composition of the upper continental crust.</p>
</caption>
<table frame="hsides">
<thead>
<tr>
<th valign="middle" align="center">Element concentrations</th>
<th valign="middle" align="center">Patagonian dust (this study)</th>
<th valign="middle" align="center">Range in Patagonian riverborne and windborne (<xref ref-type="bibr" rid="B34">Gaiero et&#xa0;al., 2003</xref>)</th>
<th valign="middle" align="center">Average in upper continental crust (<xref ref-type="bibr" rid="B111">Wedepohl, 1995</xref>)</th>
</tr>
</thead>
<tbody>
<tr>
<td valign="middle" align="left">Al (%)</td>
<td valign="middle" align="center">7.13 &#xb1; 0.85 (n=3)</td>
<td valign="middle" align="center">6.70-9.70</td>
<td valign="middle" align="center">7.74</td>
</tr>
<tr>
<td valign="middle" align="left">Fe (%)</td>
<td valign="middle" align="center">3.94 &#xb1; 0.40 (n=3)</td>
<td valign="middle" align="center">1.60-6.40</td>
<td valign="middle" align="center">3.08</td>
</tr>
</tbody>
</table>
</table-wrap>
<p>The XRD analysis method was limited in its ability to detect specific Fe minerals in Patagonian dust due to the prevalent abundance of quartz and aluminosilicates compared to other mineral species. Consequently, the XANES spectrum of the samples was employed to conduct a more comprehensive analysis of the dust, particularly regarding Fe minerals, following incubation in seawater. The analysis revealed the presence of several key Fe minerals, primarily heterosite (Fe<sup>3 +</sup> 0.65 Mn<sup>3 +</sup> 0.35)PO<sub>4</sub> (~77%), Fe(III) sulfate hydrate (~20%), and magnetite (~3%) (<xref ref-type="fig" rid="f1">
<bold>Figure&#xa0;1</bold>
</xref>). Additionally, micro-fluorescence scans were employed to assess the element concentrations of individual particles collected on filters. To enable a comparison between the elemental composition of particles obtained from micro-fluorescence measurements (<xref ref-type="fig" rid="f1">
<bold>Figure&#xa0;1</bold>
</xref>) and those analyzed by ICP-QMS, the average metal concentrations were estimated using the total area of the coarse and fine scans, corresponding to the overall surface of the filter. The initial average Fe concentration estimated on the entire filter surface was 374 nmol L<sup>-1</sup>, approximately 1.5 times lower than the values measured by ICP-QMS (~550 nmol L<sup>-1</sup> Fe). In addition, a notable inconsistency in the estimated Fe concentration was observed among the analyses from different sections of the filter. Given that the surface analyzed by micro-fluorescence was small (100 &#xb5;m&#xb2; for coarse scans and 30 &#xb5;m&#xb2; for fine scans) relative to the total filter surface (17.34 cm&#xb2;), the observed disparities among the various sections of the filter likely reflected the inherent heterogeneity in mineral distribution across the filter surface. Furthermore, the Fe/Al elemental ratio measured by ICP-QMS (Fe/Al = 0.27) differed from the ratio obtained in single particles (Fe/Al = 0.03-5.93). However, the X-ray analysis may not fully penetrate the aggregates, thus resulting in a lower Fe concentration estimation by micro-fluorescence compared to ICP-QMS measurements (<xref ref-type="bibr" rid="B98">Spolnik et&#xa0;al., 2004</xref>). Additionally, the presence of aggregates counted as a single particle could contribute to measurement inaccuracies. Among the probabilities of occurrence of such aggregates, colloids may be the most likely to create this bias as they are known for their prevalence in seawater and in dust (<xref ref-type="bibr" rid="B112">Wells and Goldberg, 1993</xref>; <xref ref-type="bibr" rid="B1">Aguilar-Islas et&#xa0;al., 2010</xref>). Moreover, small particles located on the surface of the largest particles could also affect the measurements. The elemental concentrations in each particle were ranked in the order of Si (&lt; 8000 nmol cm<sup>&#x2212;2</sup>) &gt; Al (&lt; 2000 nmol cm<sup>&#x2212;2</sup>) &gt; Fe (&lt; 1000 nmol cm<sup>&#x2212;2</sup>) (<xref ref-type="supplementary-material" rid="SM1">
<bold>Supplementary Information, Table&#xa0;3</bold>
</xref>), similar to ICP-QMS results (<xref ref-type="table" rid="T3">
<bold>Table&#xa0;3</bold>
</xref>). The notable presence of Si and Al, detected at the micrometric scale within each particle, further corroborated the findings from the XRD analysis, which indicated a predominance of aluminosilicates in the Patagonian dust (<xref ref-type="fig" rid="f2">
<bold>Figure&#xa0;2</bold>
</xref>).</p>
<fig id="f1" position="float">
<label>Figure&#xa0;1</label>
<caption>
<p>Relative mineral composition of Fe (%) in the dust incubated in seawater obtained with XANES analyses and proceed using Athena software. The standard deviation is computed based on the duplicates conducted at two distinct spots on the same filter.</p>
</caption>
<graphic mimetype="image" mime-subtype="tiff" xlink:href="fmars-11-1363088-g001.tif"/>
</fig>
<fig id="f2" position="float">
<label>Figure&#xa0;2</label>
<caption>
<p>Micro-XRF scan of dust incubated in seawater. The scan shows in detail the colocations of the three major elements of the dust, Fe (in red), Al (in green) and Si (in blue). The scan shows predominance of quartz and aluminosilicates in the Patagonian dust.</p>
</caption>
<graphic mimetype="image" mime-subtype="tiff" xlink:href="fmars-11-1363088-g002.tif"/>
</fig>
<p>Based on the elemental concentrations per particle, elemental ratios were computed to correlate them with the corresponding minerals (<xref ref-type="bibr" rid="B70">Oakes et&#xa0;al., 2012</xref>). The Si/Al elemental ratios measured in the incubated dust (<xref ref-type="supplementary-material" rid="SM1">
<bold>Supplementary Information, Table&#xa0;3</bold>
</xref>) were indicative of quartz and aluminosilicates, with values ranging from 1 to 4 (<xref ref-type="bibr" rid="B70">Oakes et&#xa0;al., 2012</xref>). Furthermore, the Fe/Al elemental ratio (<xref ref-type="supplementary-material" rid="SM1">
<bold>Supplementary Information, Table&#xa0;3</bold>
</xref>) was utilized to identify Fe-oxides, displaying values between 3 and 6 (<xref ref-type="bibr" rid="B70">Oakes et&#xa0;al., 2012</xref>). Notably, the Fe-oxides were characterized by a Fe concentration hovering 1000 &#xb5;g cm<sup>-</sup>&#xb2;. The relative abundance of these minerals was estimated, with quartz and aluminosilicates accounting for approximately ~57% and Fe-oxides comprising around ~6.9%, aligning closely with the Fe-oxide content reported in <xref ref-type="bibr" rid="B77">Qu (2016)</xref> of 6.19%.</p>
<p>In addition to exploring the mineralogy and composition of the incubated dust, investigating the redox speciation of metals within the particles is important in order to understand their dissolution in seawater. However, it has not been thoroughly investigated to date. Tracking the physico-chemical variations of the Fe mixture from its origin to its deposition in oceanic waters presents considerable challenges. Notably, the atmosphere can experience the mixing of dust from diverse sources, which may undergo varying oxidation reactions triggered by light exposure and acidification (<xref ref-type="bibr" rid="B29">Desboeufs et&#xa0;al., 2005</xref>; <xref ref-type="bibr" rid="B86">Rubasinghege et&#xa0;al., 2010</xref>). Moreover, the meteorology-dependent light radiation can significantly impact the redox speciation and the residence time of dust in the atmosphere, which can span from hours to weeks (<xref ref-type="bibr" rid="B46">Jickells et&#xa0;al., 2005</xref>). Oceanic waters can also be the place of mixing for different dust mineralogies and redox states of elements, further complexifying the scenario (<xref ref-type="bibr" rid="B89">Schulz et&#xa0;al., 2012</xref>). Thus, it is therefore imperative to define the effects of environmental parameters on the redox speciation of metals in the dust more precisely. This can be achieved through controlled laboratory experiments that allow for a more comprehensive assessment of the underlying processes. To this end, XANES analyses of the filter area were performed to characterize the Fe redox speciation in both dry and incubated dust. The Fe(II)/Fe(III) ratio in Patagonian dust was determined to be 0.25, with ~20 &#xb1; 1.42% of Fe(II), which corresponds to the reported atmospheric ranges of 5 to 35% (average of 25%) (<xref ref-type="bibr" rid="B70">Oakes et&#xa0;al., 2012</xref>), and with marine aerosols (less than 73%) (<xref ref-type="bibr" rid="B99">Takahama et&#xa0;al., 2008</xref>). The ratio of Fe(II) to Fe(III) within particles can serve as a proxy for assessing their crustal origin (low Fe(II)), and of its volcanic and/or anthropogenic sources (up to 98%), in conjunction with their element composition (<xref ref-type="bibr" rid="B70">Oakes et&#xa0;al., 2012</xref>; <xref ref-type="bibr" rid="B97">Spolaor et&#xa0;al., 2013</xref>), indicating the lithogenic origin of Patagonian dust. The recorded relative abundance of Fe(II) in Patagonian dust (20%) was in the upper range of the crustal signature. Our findings, in line with previous studies (<xref ref-type="bibr" rid="B91">Shi et&#xa0;al., 2012</xref>), suggested that the value of Fe(II)/Fe(III) ratio can be used as an effective tracer for discerning the origin of the desertic dust that can persist over time.</p>
</sec>
<sec id="s4_2">
<label>3.2</label>
<title>Kinetics of the dissolution of Fe from the Patagonian dust</title>
<p>During the dust dissolution experiments in seawater, there was no indication of a higher dissolution rate of one Fe-mineral relative to the others (<xref ref-type="fig" rid="f1">
<bold>Figure&#xa0;1</bold>
</xref>). In fact, the predominant heterosites, characterized by an orthorhombic dipyramidal system (<xref ref-type="bibr" rid="B32">Fehr et&#xa0;al., 2010</xref>) are isostructural with the anhydrous Fe sulfate (FeSO<sub>4</sub>), even though FeSO<sub>4</sub> can manifest itself in various forms, such as monohydrate, tetrahydrate and heptahydrate (<xref ref-type="bibr" rid="B87">Ruggiero et&#xa0;al., 2015</xref>). Therefore, given their analogous structural nature, these minerals may exhibit similar behavior in seawater, without any discernible trend of relative dissolution over time. Owing to their ordered structure, the reactivity may be relatively low (<xref ref-type="bibr" rid="B101">Toner et&#xa0;al., 2012</xref>), thus indicating a prolonged lifespan for Fe minerals from Patagonian dust in seawater. These Fe-minerals can be indeed classified as minerals with a long reaction time, extending beyond a week (<xref ref-type="bibr" rid="B75">Poulton et&#xa0;al., 2004</xref>). For instance, the half-life time of magnetite in seawater at pH 7.5 is 72 days (<xref ref-type="bibr" rid="B75">Poulton et&#xa0;al., 2004</xref>). Furthermore, when dust minerals come into contact with seawater, substitutions of elements within the mineral structure might occur, yet these effects have minimal impact on the reactivity of the minerals (<xref ref-type="bibr" rid="B75">Poulton et&#xa0;al., 2004</xref>). Moreover, in the two predominant Fe-minerals found in the Patagonian dust (heterosites and Fe(III) sulfate hydrate), the associated elements with Fe were PO<sub>4</sub> and SO<sub>4</sub>, both of which are abundant constituents (PO<sub>4</sub> ~2 &#xb5;mol L<sup>-1</sup>, SO<sub>4</sub> ~2.67 mg L<sup>-1</sup>) in the seawater of the SO (<xref ref-type="bibr" rid="B12">Brandini et&#xa0;al., 2000</xref>; <xref ref-type="bibr" rid="B67">Naik et&#xa0;al., 2006</xref>). Thus, these minerals may exhibit reduced solubility owing to the relatively high concentrations of PO<sub>4</sub> and SO<sub>4</sub> in seawater, thereby slowing down the dissolution process and rendering these minerals less reactive. Additionally, no discernible mineralogical distinctions were observed between the present and projected future conditions (ANOVA test, heterosite: p-value= 0.09, Fe(III) sulfate hydrate: p-value = 0.10, magnetite: p-value = 0.88; <xref ref-type="fig" rid="f1">
<bold>Figure&#xa0;1</bold>
</xref>), implying that changes in temperature, pH, and PAR are unlikely to significantly impact the Fe mineralogy within the dust. Thus, our results regarding the particulate fraction, suggested that the incubated Patagonian dust might be relatively less affected by anticipated environmental changes in the future SO. Crystalline systems, unless disrupted, can retain their constituent elements within their structure, preventing their release into the surrounding environment (<xref ref-type="bibr" rid="B103">Totsche et&#xa0;al., 2018</xref>). The environmental changes in the SO did not appear to reach extreme thresholds capable of disrupting the minerals, either during the experimental period of a week or under the future environmental conditions. Nevertheless, biological activities of autotrophs and heterotrophs in ambient seawaters could trigger mechanisms capable of destroying these minerals (<xref ref-type="bibr" rid="B83">Reinl et&#xa0;al., 2022</xref>). This includes the production of organic ligands complexing with dFe, thereby competing with Fe scavenging on dust particles (<xref ref-type="bibr" rid="B114">Wuttig et&#xa0;al., 2013</xref>), although such processes were not emulated in these abiotic experiments. Additionally, it is important to acknowledge that seasonal fluctuations and daily variations might significantly impact the Fe in Patagonian dust, potentially exceeding the magnitude of changes between the experimental present and future conditions. While Patagonian aerosols could release colloidal and soluble materials, potentially influencing seawater composition, but the reverse influence of seawater on the mineralogy of these dust particles is likely limited.</p>
<p>All samples showed identical XANES spectra, regardless of the dry or incubated dust, the sampling time, or the experimental conditions (pink curve on <xref ref-type="fig" rid="f3">
<bold>Figure&#xa0;3</bold>
</xref>). The consistent Fe(II)/Fe(III) ratio observed at the pre-edge (<xref ref-type="fig" rid="f3">
<bold>Figure&#xa0;3</bold>
</xref>) suggested that environmental changes, such as an increase in PAR that can impact photochemical reactions (<xref ref-type="bibr" rid="B33">Fu et&#xa0;al., 2010</xref>), did not affect the redox speciation of Fe in the particles. However, it is possible that the one-week incubation period was insufficient to induce any discernible alterations in the Fe redox speciation (<xref ref-type="bibr" rid="B60">Mayhew et&#xa0;al., 2011</xref>). Another explanation is that certain oxidation/reduction processes occurred within a very short time scale, such as during the sample filtration, when Fe(II) might have been rapidly oxidized to Fe(III), making it challenging to capture the initial redox speciation of Fe. Additionally, the time between the incubation and the sample measurement was 3 months, possibly affecting the observed results. It is also possible that the rate of redox conversions between Fe(III) and Fe(II) were too low to be detected within the one-week experimental duration. However, the conversion of particulate Fe(III) to Fe(II) remains elusive, as these processes have been more extensively investigated in the dissolved fraction (<xref ref-type="bibr" rid="B48">Kappler and Newman, 2004</xref>). Furthermore, the absence of biological activity in our experiments, especially the absence of biological production of organic ligands and chromophores capable of reducing Fe(III) under light (<xref ref-type="bibr" rid="B4">Barbeau, 2006</xref>) may have limited the change in the redox speciation of Fe.</p>
<fig id="f3" position="float">
<label>Figure&#xa0;3</label>
<caption>
<p>Average of XANES spectra of the all samples (purple) and associated Fe standards selected among 26 references by linear combination fitting.</p>
</caption>
<graphic mimetype="image" mime-subtype="tiff" xlink:href="fmars-11-1363088-g003.tif"/>
</fig>
<p>On the other hand, the dissolution of Fe from incubated Patagonian dust in seawater under present and future conditions was assessed by following the pFe concentration over time of incubation. The particulate trace metals concentrations in the filtered seawater prior to dust addition was below detection limits of ICP-QMS measurements (&lt;1 nmol L<sup>-1</sup>). Then, the pFe concentration in seawater 3 min after the dust addition (~532 nmol L<sup>-1</sup> Fe in current condition) was in the range of the estimated total Fe in the 1 mg L<sup>-1</sup> of added dust for the present scenario (~624 nmol Fe mg<sup>-1</sup>) and 1076 nmol L<sup>-1</sup> Fe in future condition. The discrepancy of approximately 92 nmol L<sup>-1</sup> might be attributed to uncertainties on the weighted dust and the volume of seawater used for the experiments. Nonetheless, this difference did not affect the interpretation of the dissolution kinetics.</p>
<p>Under the present conditions, pFe increased by ~50 nmol L<sup>-1</sup> over the first 1H30, reaching a peak value of 585 nmol L<sup>-1</sup> (<xref ref-type="fig" rid="f4">
<bold>Figure&#xa0;4</bold>
</xref>). Then, the concentration decreased, returning to its initial value within another 1H30 period. A third phase of dissolution started after this initial period of 3 hours, characterized by a slow decrease in pFe of 150 nmol L<sup>-1</sup> over the course of one week. Under the future condition, the timing and the changes in particulate concentrations were slightly different. Particulate Fe increased by 60 nmol L<sup>-1</sup> during the initial 3 hours of the experiment, without an immediate rapid decline. Instead, a gradual decrease in pFe began immediately and showed an amplitude of 200 nmol L<sup>-1</sup>.</p>
<fig id="f4" position="float">
<label>Figure&#xa0;4</label>
<caption>
<p>Kinetic of dissolution of pFe from Patagonian dust in seawater at the present and future environmental conditions during the first hours (top panel) and over 7 days (bottom panel). The measured pFe concentration without dust addition corresponds to ~1.3 nmol L<sup>-1</sup>. Standard deviations are calculated from 5 analysis replicates.</p>
</caption>
<graphic mimetype="image" mime-subtype="tiff" xlink:href="fmars-11-1363088-g004.tif"/>
</fig>
<p>To elucidate the observed pFe dynamics depicted in <xref ref-type="fig" rid="f4">
<bold>Figure&#xa0;4</bold>
</xref>, SEM observations of incubated dust were conducted at different times of incubation and under the two conditions (<xref ref-type="fig" rid="f5">
<bold>Figure&#xa0;5</bold>
</xref>). The SEM analyses revealed a higher incidence of particles with colloids adsorbed to their surfaces, as well as aggregates of particles during the first hours of the kinetics. After one day of incubation, a greater number of dust particles exhibiting a polished surface were identified. No discernible difference was observed in the prevalence of these various particle types and aggregates between the present and future conditions. However, it is important to note that the qualitative assessment of the dust nature using SEM imaging posed challenges in terms of quantitative analysis, and a significant level of uncertainty persisted.</p>
<fig id="f5" position="float">
<label>Figure&#xa0;5</label>
<caption>
<p>SEM observation of Patagonian dust in current condition; colloids at the surface of the particle <bold>(A)</bold> at the time of dust addition, <bold>(B)</bold> an agglomerate of colloids (first few hours), <bold>(C)</bold> and an aggregate of colloidal and particulate dust, <bold>(D)</bold> particle with a flat surface after 5 days.</p>
</caption>
<graphic mimetype="image" mime-subtype="tiff" xlink:href="fmars-11-1363088-g005.tif"/>
</fig>
<p>The initial phase of the kinetics was characterized by an unexpected increase in the concentration of the particulate fraction. In an effort to elucidate the behavior of the Patagonian dust in seawater, the aerodynamic model of <xref ref-type="bibr" rid="B90">Shao (2008)</xref> was adapted (<xref ref-type="fig" rid="f6">
<bold>Figure&#xa0;6</bold>
</xref>). This model categorizes particle behavior based on size classes, indicating that the finest atmospheric particles (&lt;2 &#xb5;m) can aggregate as observed in the SEM pictures, a characteristic that corresponds with the distribution of the majority of particles from the Patagonian dust (<xref ref-type="bibr" rid="B95">Sow et&#xa0;al., 2009</xref>). For instance, the increase of pFe concentration that has been observed shortly after a dust deposition in a Mediterranean mesocosm coincided with a decrease in dFe, and was attributed to the scavenging of dFe onto the dust particles (<xref ref-type="bibr" rid="B108">Wagener et&#xa0;al., 2010</xref>). The formation of Patagonian dust aggregates in seawater may be facilitated under conditions of low ionic strength owing to the bonds with dissolved organic matter (<xref ref-type="bibr" rid="B18">Chekli et&#xa0;al., 2015</xref>) or via polymeric effects and Van der Waals forces that neutralize the negative charges on the surface of the particles, resulting in an attractive effect (<xref ref-type="bibr" rid="B113">Winterwerp and van Kesteren, 2004</xref>). Thus, the use of seawater fostered aggregate formation, allowing for the slow establishment of equilibrium between the seawater and the metals, an equilibrium that can extend over a week or more (<xref ref-type="bibr" rid="B25">Deguillaume et&#xa0;al., 2005</xref>). In addition, labile Fe was unable to coagulate with particulate organic matter, given that seawater was filtered at 0.2 &#x3bc;m, thereby preventing the generation of organic matter in seawater during storage and experimentation. Conversely, the dissolved organic matter originally present in the water might have played a significant role in facilitating dissolution by forming Fe-binding ligands (<xref ref-type="bibr" rid="B14">Bressac and Guieu, 2013</xref>). Furthermore, the adsorption of small colloids onto the particles is also a plausible contributing factor as observed in the SEM scans, as the leached dFe from natural aerosols is generally dominated by the colloid fraction (<xref ref-type="bibr" rid="B1">Aguilar-Islas et&#xa0;al., 2010</xref>). Indeed, with an addition of about 532 nmol L<sup>-1</sup> of pFe, the concentrations were well above the concentration of the Fe solubility limit (~0.2-0.3 nmol L<sup>-1</sup>) for Fe(III) in seawater (<xref ref-type="bibr" rid="B65">Millero, 1998</xref>). Even when compared to a natural input that could be 10 or 100 times lower than the concentration employed in this experiment (<xref ref-type="bibr" rid="B42">Heimburger et&#xa0;al., 2012</xref>), the Fe concentration would still exceed the solubility limit. Therefore, this experiment accurately replicates realistic physicochemical processes. Knowing that the dissolved fraction was Fe-saturated by the supply of Patagonian dust, and that no organic ligands were produced in these experiments, most of the released Fe would have been in the form of inorganic complex and colloids (<xref ref-type="bibr" rid="B11">Boye et&#xa0;al., 2005</xref>), thereby promoting colloid formation. Consequently, the increase of pFe at the beginning of the kinetics could be linked to the formation of colloids and aggregates, and the adsorption of colloids on the particle surfaces, thus impeding the dissolution of the dust mantle by providing a shelter for the surface area, thereby reducing its contact with water. It is also conceivable that the time step used in this experiment might have hindered the observation of any rapid dissolution processes occurring within the initial minutes of dust incubation (<xref ref-type="bibr" rid="B109">Wagener et&#xa0;al., 2008</xref>).</p>
<fig id="f6" position="float">
<label>Figure&#xa0;6</label>
<caption>
<p>Conceptual schematic of the Patagonian dust dissolution process in seawater (using <uri xlink:href="https://www.BioRender.com">BioRender</uri>) after <xref ref-type="bibr" rid="B90">Shao, 2008</xref>.</p>
</caption>
<graphic mimetype="image" mime-subtype="tiff" xlink:href="fmars-11-1363088-g006.tif"/>
</fig>
<p>After 1H30, the concentration rapidly decreased in the particulate phase, exhibiting a temporal and quantitative magnitude comparable to the preceding increase. The rupture of bonds and cohesive forces between colloids aggregates and between colloids and particles could explain such decrease. After extended contact with seawater, the dissolution process would initiate within a thin surface layer of particles and colloids. Here, surface segregation mechanisms (<xref ref-type="bibr" rid="B26">Delage, 1998</xref>) might accelerate dissolution at the surface compared to inside of the particles, given that the diffusion of elements is quicker in the surface layers than within the particle volume. Subsequently, as this surface layer dissolves, the cohesive forces between the particles would weaken, leading to the disintegration of the aggregates.</p>
<p>After 3 hours, the dissolution rate decelerated, marking the onset of the third phase of dissolution in Patagonian dust. This pattern of dissolution was akin to the dissolution of Saharan dust in Mediterranean waters, where a slower dissolution phase started after 2.6 hours (<xref ref-type="bibr" rid="B109">Wagener et&#xa0;al., 2008</xref>). The deceleration can be attributed to the complete dissolution of the surface thin layer of dust (<xref ref-type="bibr" rid="B28">Desboeufs, 2001</xref>), resulting in the collapse of colloid aggregates due to diminished cohesive forces. Subsequently, a new dissolution phase initiated, affecting the core of the particles. This dissolution was much slower than the second phase as it involves the most refractory part of the dust (<xref ref-type="bibr" rid="B28">Desboeufs, 2001</xref>).</p>
</sec>
<sec id="s4_3">
<label>3.3</label>
<title>Dissolution rates and residence time of Patagonian Fe dust</title>
<p>The dissolution rate of pFe was calculated during the third dissolution phase, following the <xref ref-type="disp-formula" rid="eq3">Equation 3</xref>, where PTm<sub>ti</sub> is the pFe concentration at the start of this phase (ti) and PTm<sub>tf</sub> after 7 days of incubation (tf).</p>
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<p>The dissolution rate was subsequently divided by the total quantity of metal present in the dust and converted into a percentage (<xref ref-type="disp-formula" rid="eq4">Equation 4</xref>).</p>
<disp-formula id="eq4">
<label>(4)</label>
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<p>Based on these calculations, we estimated the Fe dissolution rate from the Patagonian dust to be around 18.9 nmol L<sup>-1</sup> day<sup>-1</sup> (3.6% day<sup>-1</sup>) during the third phase of the dissolution kinetic in the current conditions. The dissolution of Fe can also be affected by the origin of particles and the medium of dissolution. For instance, the observed Fe dissolution rate was lower than those reported for Patagonian dust in Milli-Q water, which reached up to 9% within 15 minutes (<xref ref-type="bibr" rid="B77">Qu, 2016</xref>). The dissolution rate of Fe-dust was also lower than those found in Kerguelen Islands, a deposition site for Patagonian dust, where the dissolution rates were measured at 82 &#xb1; 18% in rainwater (<xref ref-type="bibr" rid="B41">Heimburger et&#xa0;al., 2013a</xref>). The comparatively higher dissolution rates in Milli-Q water and rainwater compared to seawater might be attributed to the acidic conditions. On the other hand, the rates of Patagonian dust dissolution were higher than those recorded for the Saharan aerosol, which exhibited a dissolution rate of approximately ~0.9 nmolFe day<sup>-1</sup> (0.02% in 3 days) (<xref ref-type="bibr" rid="B109">Wagener et&#xa0;al., 2008</xref>), or 0.05 to 2.2% per day (<xref ref-type="bibr" rid="B8">Bonnet and Guieu, 2004</xref>), albeit the Saharan dust containing more Fe (~5%; <xref ref-type="bibr" rid="B62">Mendez et&#xa0;al., 2010</xref>) compared to Patagonian dust (~3.94%, this study), and therefore expected to have a higher dissolution rate. In addition, our study used half the amount of dust compared to the study of <xref ref-type="bibr" rid="B8">Bonnet and Guieu (2004)</xref>, which may not explain the higher dissolution rate observed for Fe from Patagonian dust. Consequently, the discrepancy between our dissolution rate and other studies could primarily be attributed to the nature of the dust (whether it contains Fe in aluminosilicate, Fe-oxide, and amorphous Fe) and the variation in size class distribution. Saharan soils typically are composed of larger grain sizes, averaging around 10-20 &#xb5;m (<xref ref-type="bibr" rid="B39">Guieu et&#xa0;al., 2002</xref>), which could potentially impede the dissolution process. However, the absence of a detailed mineralogical analysis of the dust used for the Saharan aerosol dissolution hampers a comprehensive understanding of the difference dissolution rate of Fe-dust. The methodology employed could also offer insights into these observed differences. Unlike prior investigations, which primarily focused on tracking dissolution rates within the dissolved fraction alone, this study extends its analysis to encompass the particulate fraction. Consequently, our experimental approach may provide a more comprehensive assessment of dissolution dynamics, capturing the transition of Fe &#xa0;from the particulate phase to the dissolved phase. Notably, monitoring dissolution solely within the dissolved fraction&#xa0;overlooks the potential complexation by organic and inorganic ligands, thereby omitting a significant aspect of dissolution behavior.</p>
<p>Conversely, in the future scenario, the dissolution rate was slower with ~19.4 nmol L<sup>-1</sup> day<sup>-1</sup> (1.8% day<sup>-1</sup>). The variations in dissolution rates observed between the present and future conditions can be attributed by changes in experimental factors. For instance, during the last glacial maximum, Fe solubility of atmospheric dust in the SO exhibited high variability, ranging from 1 to 42%, with inputs 10 fold higher than modern deposition (<xref ref-type="bibr" rid="B20">Conway et&#xa0;al., 2015</xref>). Consequently, Fe dissolution can be impacted by a multitude of physical, chemical, and biological parameters and is likely to evolve under the influence of anthropogenic alterations (<xref ref-type="bibr" rid="B93">Shi et&#xa0;al., 2011</xref>). The experimental changes, such as temperature, pH, PAR, and the quantity of added dust, might account for the observed differences in dissolution between the present and future conditions.</p>
<p>For example, the anticipated increase of PAR in the future condition from 30 &#xb1; 6 to 55 &#xb1; 7 &#x3bc;mol quanta m<sup>-2</sup> s<sup>-1</sup> (<xref ref-type="bibr" rid="B10">Boyd et&#xa0;al., 2016</xref>), is expected to intensify photochemical reactions, thereby rendering trace metals more soluble, and consequently augmenting Fe dissolution. However, photoreduction predominantly occurs at low pH levels of 2.5-5 (<xref ref-type="bibr" rid="B31">Faust and Hoign&#xe9;, 1990</xref>), which was not the case in the future scenario, as the reactions were taking place at the future basic pH of seawater.</p>
<p>Regarding the impact of pH, the common assumption would be that the dissolution should be magnified under more acidic pH conditions due to the increased concentration of H<sup>+</sup> ions, leading to a protonation process that weakens the Fe-O bonds on the particle surface, thus causing the release of Fe from the oxidic bulk (<xref ref-type="bibr" rid="B21">Cornell and Schwertmann, 2003</xref>). For example, the solubility of Fe in aerosols was shown to increase in Milli-Q water with decreasing pH, from 0.1% at pH 8 to 0.3% at pH 5.5 and to 4.7% at pH 2 (<xref ref-type="bibr" rid="B96">Spokes and Jickells, 1996</xref>). Furthermore, the solubility of Fe was found to be lower in the pH range of 7.5 to 9 compared to acidic conditions, and it varied only minimally within this range (<xref ref-type="bibr" rid="B52">Liu and Millero, 2002</xref>). Considering the projected shift of the seawater pH from 8.10 to 7.80 by 2100, the pH would not significantly impact the Fe solubility in our experiment. This result contrasts with what was previously suggested by <xref ref-type="bibr" rid="B105">Trimborn et&#xa0;al. (2017)</xref> indicating acidification could increase the Fe dissolution in combination with biological activity. A study (<xref ref-type="bibr" rid="B13">Breitbarth et&#xa0;al., 2010</xref>) investigating changes in the Fe speciation under varying CO<sub>2</sub> treatments, revealed that the increase of dFe in coastal waters was predominantly governed by biological factors compared to acidification, particularly the stability of Fe-ligand complexes.</p>
<p>Next, the dissolution of dust could be amplified with increasing temperature due to the entropy agitation of the particles in the liquid. Nevertheless, the solubility of Fe decreases in seawater with rising temperature (<xref ref-type="bibr" rid="B52">Liu and Millero, 2002</xref>). Consequently, the projected +3&#xb0;C increase in future conditions could be a contributing factor to the observed lower dissolution rate compared to present conditions.</p>
<p>Furthermore, the twofold increase in dust input in the experimental future condition likely led to an increase in aggregate formation, consequently reducing the surface-to-volume ratio of the dust particles. Such surface-to-volume decrease can result in lowering the exchange surface area, lead to a decrease of Fe dissolution, as previously observed with an increase in particle concentration (<xref ref-type="bibr" rid="B6">Biscombe, 2004</xref>) and when the dust concentration was lower than 20 mg L<sup>-1</sup> (<xref ref-type="bibr" rid="B96">Spokes and Jickells, 1996</xref>). Additionally, the introduction of dust could lead to a reduction in dFe due to the adsorption of dFe on the dust particles and the formation of aggregates (<xref ref-type="bibr" rid="B108">Wagener et&#xa0;al., 2010</xref>). After deposition, atmospheric Fe exhibited a tendency to scavenge onto particles, particularly in conditions where concentrations of both particles and dissolved organic matter were elevated (<xref ref-type="bibr" rid="B14">Bressac and Guieu, 2013</xref>).</p>
<p>In summary (<xref ref-type="table" rid="T4">
<bold>Table&#xa0;4</bold>
</xref>), the synergistic effect of the combined experimental parameters in the future conditions lead to the observed ~50% reduction in the dissolution rate by the end of the century.</p>
<table-wrap id="T4" position="float">
<label>Table&#xa0;4</label>
<caption>
<p>Potential drivers that can control the dissolution of Fe from Patagonian dust in present and future seawater of the SO. (+) means increase of the dissolution, (-) means decrease of the dissolution and (~) means no significant impact.</p>
</caption>
<table frame="hsides">
<thead>
<tr>
<th valign="middle" align="left">Drivers</th>
<th valign="middle" align="center">Dust concentration</th>
<th valign="middle" align="center">Temperature</th>
<th valign="middle" align="center">pH</th>
<th valign="middle" align="center">PAR</th>
</tr>
</thead>
<tbody>
<tr>
<td valign="top" align="left">Present day condition</td>
<td valign="middle" align="center">+</td>
<td valign="middle" align="center">+</td>
<td valign="middle" align="center">~</td>
<td valign="middle" align="center">~</td>
</tr>
<tr>
<td valign="top" align="left">Future condition</td>
<td valign="middle" align="center">&#x2013;</td>
<td valign="middle" align="center">&#x2013;</td>
<td valign="middle" align="center">~</td>
<td valign="middle" align="center">+</td>
</tr>
</tbody>
</table>
</table-wrap>
<p>The residence time of pFe in a stratified mixed-layer was estimated using the sinking rate of dust particles in seawater. The&#xa0;sinking rate was calculated using <xref ref-type="disp-formula" rid="eq5">Equation 5</xref> (<xref ref-type="bibr" rid="B71">Omand et&#xa0;al., 2020</xref>), which includes w<sub>sink</sub> (velocity of the particle; m s<sup>-1</sup>), g (acceleration due to the gravity; m s<sup>-2</sup>), r (radius of the particle; m), &#x3c1;<sub>particle</sub> (density of the particle; kg m<sup>-3</sup>), &#x3c1;<sub>seawater</sub> (density of seawater; kg m<sup>-3</sup>), n<sub>seawater</sub> (kinematic viscosity of seawater; kg m<sup>-1</sup> s<sup>-1</sup>). As the density of the Patagonian dust was not measured in this study, a global average value (~2600 kg m<sup>-3</sup>) for desert dust particles was adopted (<xref ref-type="bibr" rid="B110">Wagner et&#xa0;al., 2009</xref>).</p>
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<p>Depending of the particle size, the residence time in the mixed layer can be highly versatile (<xref ref-type="bibr" rid="B106">van der Jagt et&#xa0;al., 2018</xref>). Applying the equation yielded an estimated residence time for the largest particles (~10 &#xb5;m) of 14 days in a 89 m mixed layer (HNLC) and 8 days in a 50 m mixed layer (Polar Frontal Zone) (<xref ref-type="bibr" rid="B23">De Boyer Mont&#xe9;gut et&#xa0;al., 2004</xref>). However, considering the size distribution of Patagonian dust, which is centered at around 2-5 &#xb5;m and 0.3-0.5 &#xb5;m, the calculated residence times were 112 days and 24 years in HNLC and 63 days and 14 years in the PFZ, respectively. Based on the dissolution rates obtained in our study, the Fe content of Patagonian dust would be completely dissolved in 26 days under present conditions and in 55 days under future conditions. Therefore, most of the Fe dissolved from the dust can remain in the mixed-layer depth. Therefore, in future anticipated condition with a doubling of pFe inputs and a 50% reduction in dissolution rate, an equivalent quantity of dFe is expected to be released from dust, potentially becoming bioavailable to phytoplankton. With a dust flux from South America to the SO region of 0.3 mg m<sup>-</sup>&#xb2; d<sup>-1</sup> (<xref ref-type="bibr" rid="B51">Li et&#xa0;al., 2008</xref>), and a mean Fe concentration in Patagonian dust of ~3.94% (this study), the atmospheric deposition flux of Fe from dust would be to around ~0.011 mgFe m<sup>-</sup>&#xb2; d<sup>-1</sup>. Using the observed dissolution rate of 3.6% d<sup>-1</sup> in the current conditions, this input would represent a flux of dFe of 0.43 &#xb5;gFe m<sup>-</sup>&#xb2; d<sup>-1</sup> (7.62 nmol m<sup>-</sup>&#xb2; d<sup>-1</sup>) in the surface waters of the SO (<xref ref-type="disp-formula" rid="eq6">Equation 6</xref>). With an expected doubled input of Patagonian dust in the future conditions, the dissolution rates we recorded was 1.8% d<sup>-1</sup>, leading to a corresponding flux of dFe in seawater of 0.43 &#xb5;gFe m<sup>-</sup>&#xb2; d<sup>-1</sup> (7.6 nmol m<sup>-</sup>&#xb2; d<sup>-1</sup>).</p>
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</disp-formula>
<p>The flux of dFe in the mixed layer found under present and future conditions correspond to 0.09 pmolFe L<sup>-1</sup> d<sup>-1</sup> in HNLC and 0.15 pmolFe L<sup>-1</sup> d<sup>-1</sup> in PFZ (<xref ref-type="disp-formula" rid="eq7">Equation 7</xref>, in which the mixed layer depth was 89 m in the HNLC area and 50 m in the PFZ). Despite the projected doubling of dust input in the future, the impact of environmental changes was shown to lead to a 2-fold reduction in Fe dissolution rate. As a result, the dFe concentrations are not anticipated to increase in future projections.</p>
<disp-formula id="eq7">
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<p>The estimated dFe inputs obtained in this study were 0.09 pmol L<sup>-1</sup> d<sup>-1</sup> in HNLC for both conditions and 0.15 pmolFe L<sup>-1</sup> d<sup>-1</sup> in PFZ for both conditions.</p>
</sec>
</sec>
<sec id="s5" sec-type="conclusions">
<label>4</label>
<title>Conclusion</title>
<p>Throughout its journey from source to sink, desert dust from Patagonia undergoes the synergistic effect of various physical and biogeochemical factors, both in the atmosphere and at its contact with the marine environment. This study focused on the dust dynamics after its deposition in seawater.</p>
<p>Initial XRD analyses of the Patagonian dust unveiled the prevalence of silicate minerals, primarily quartz and plagioclase. Further synchrotron analyses highlighted the occurrence of Fe minerals, mainly as heterosites and Fe(III) sulfate hydrates within the dust particles and indicated 20% of Fe(II). The mineralogy and the Fe(II)/Fe(III) ratio were similar in both the dry and incubated dust, with no significant alteration upon submersion in seawater or exposure to future environmental changes.</p>
<p>Despite the absence of mineralogical changes, the examination of pFe indicated that Patagonian dust undergoes dissolution, releasing Fe in seawater. Specifically, the Fe dissolution rates of Patagonian dust in seawater were estimated at 3.8% d<sup>-1</sup> in the present conditions and twice less (1.6% d<sup>-1</sup>) in the future scenario (<xref ref-type="fig" rid="f7">
<bold>Figure&#xa0;7</bold>
</xref>). These dissolution rates resulted in a dFe flux of 0.09 pmol L<sup>-1</sup> d<sup>-1</sup> in the HNLC region and 0.15 pmol L<sup>-1</sup> d<sup>-1</sup> in the PFZ. Despite the anticipated doubling of dust input in the future, the slower rate of Fe dissolution negated any significant increase in dFe by 2100, with probably no significant impact to alleviate the Fe limitation in the future SO.</p>
<fig id="f7" position="float">
<label>Figure&#xa0;7</label>
<caption>
<p>Conceptual scheme of Patagonian dust dissolution under present and future Southern Ocean conditions.</p>
</caption>
<graphic mimetype="image" mime-subtype="tiff" xlink:href="fmars-11-1363088-g007.tif"/>
</fig>
<p>This study underscores the critical role of synchrotron techniques in unrevealing the intricate connections between mineralogy, redox speciation, and Fe-dust dissolution in seawater. Future research should focus on smaller size fractions (&lt;0.2 &#xb5;m) since nanoparticles exhibit distinct physicochemical properties and significantly heightened reactivity due to their high surface area-to-volume ratio. Another avenue for exploration could be to quantify the labile fraction of potentially bioavailable Fe in dust and compare these findings with the dissolution of pFe in seawater. The labile fraction is generally evaluated by acid treatment (<xref ref-type="bibr" rid="B5">Berger et&#xa0;al., 2008</xref>), a process that can yield distinct results from the dissolution of dust in seawater under baseline pH conditions.</p>
<p>The insights garnered from this study offer valuable information for the development of SO biogeochemical models, contributing to a comprehensive understanding of the intricate dynamics underlying Fe dissolution rates from Patagonian dust under present and projected environmental conditions.</p>
</sec>
<sec id="s6" sec-type="data-availability">
<title>Data availability statement</title>
<p>The original contributions presented in the study are included in the article/<xref ref-type="supplementary-material" rid="SM1">
<bold>Supplementary Material</bold>
</xref>. Further inquiries can be directed to the corresponding author.</p>
</sec>
<sec id="s7" sec-type="author-contributions">
<title>Author contributions</title>
<p>CD: Conceptualization, Data curation, Formal analysis, Investigation, Methodology, Software, Writing &#x2013; original draft, Writing &#x2013; review &amp; editing, Validation, Visualization. MB: Funding acquisition, Resources, Supervision, Visualization, Writing &#x2013; original draft, Writing &#x2013; review &amp; editing, Conceptualization, Project administration, Validation. BL: Formal analysis, Writing &#x2013; review &amp; editing. PBu: Data curation, Formal analysis, Writing &#x2013; review &amp; editing. YF: Conceptualization, Supervision, Writing &#x2013; review &amp; editing. RL: Formal analysis, Supervision, Writing &#x2013; review &amp; editing. SB: Formal analysis, Writing &#x2013; review &amp; editing. PBe: Writing &#x2013; review &amp; editing.</p>
</sec>
</body>
<back>
<sec id="s8" sec-type="funding-information">
<title>Funding</title>
<p>The author(s) declare financial support was received for the research, authorship, and/or publication of this article. This work was conducted in the framework of the SAGAS project (Solubility of Patagonian dust in the future Southern Ocean, PI MB) funded by IDEX-Universit&#xe9; Paris Cit&#xe9;. CD benefited from an international mobility grant from the STEP&#x2019;UP doctoral school of IPGP. The PhD grant of CD was funded by the University Paris Cit&#xe9;. ICP-QMS and SEM analyses were supported by IPGP analytical platform PARI (Plateforme d&#x2019;analyse haute r&#xe9;solution). This research used resources of the Advanced Photon Source, a U.S. Department of Energy (DOE) Office of Science user facility operated for the DOE Office of Science by Argonne National Laboratory under Contract No. DE-AC02-06CH11357.</p>
</sec>
<ack>
<title>Acknowledgments</title>
<p>The authors thank Ellery Ingall for kindly providing the Fe mineral standards to process the micro-XANES data. The authors thank Sophie Nowak (UPC) for XRD acquisitions.</p>
</ack>
<sec id="s9" sec-type="COI-statement">
<title>Conflict of interest</title>
<p>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.</p>
</sec>
<sec id="s10" sec-type="disclaimer">
<title>Publisher&#x2019;s note</title>
<p>All claims expressed in this article are solely those of the authors&#xa0;and do not necessarily represent those of their affiliated organizations, or those of the publisher, the editors and the reviewers. Any product that may be evaluated in this article, or claim that may be made by its manufacturer, is not guaranteed or endorsed by the publisher.</p>
</sec>
<sec id="s11" sec-type="supplementary-material">
<title>Supplementary material</title>
<p>The Supplementary Material for this article can be found online at: <ext-link ext-link-type="uri" xlink:href="https://www.frontiersin.org/articles/10.3389/fmars.2024.1363088/full#supplementary-material">https://www.frontiersin.org/articles/10.3389/fmars.2024.1363088/full#supplementary-material</ext-link>
</p>
<supplementary-material xlink:href="DataSheet_1.docx" id="SM1" mimetype="application/vnd.openxmlformats-officedocument.wordprocessingml.document"/>
</sec>
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