# Transient fertilization of a post-Sturtian Snowball ocean margin with dissolved phosphate by clay minerals

Ernest Chi Fru, Jalila Al Bahri, Christophe Brosson, Olabode Bankole, Jérémie Aubineau, Abderrazak El Albani, Alexandra Nederbragt, Anthony Oldroyd, Alasdair Skelton, Linda Lowhagen, et al.

<figure><img src="image_1.png" /></figure>

## To cite this version:

Ernest Chi Fru, Jalila Al Bahri, Christophe Brosson, Olabode Bankole, Jérémie Aubineau, et al. Transient fertilization of a post-Sturtian Snowball ocean margin with dissolved phosphate by clay minerals. Nature Communications, 2023, 14 (1), pp.8418. 10.1038/s41467-023-44240-9. hal-04520815

HAL Id: hal-04520815

https://hal.science/hal-04520815

Submitted on 26 Mar 2024

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# Transient fertilization of a post-Sturtian Snowball ocean margin with dissolved phosphate by clay minerals

Ernest Chi Fru, Jalila Al Bahri, Christophe Brosson, Olabode Bankole, Jérémie Aubineau, Abderrazak El Albani, Alexandra Nederbragt, Anthony Oldroyd, Alasdair Skelton, Linda Lowhagen, et al.

<figure><img src="image_1.png" /></figure>

## To cite this version:

Ernest Chi Fru, Jalila Al Bahri, Christophe Brosson, Olabode Bankole, Jérémie Aubineau, et al. Transient fertilization of a post-Sturtian Snowball ocean margin with dissolved phosphate by clay minerals. Nature Communications, 2023, 14 (1), pp.8418. 10.1038/s41467-023-44240-9. hal-04520815

HAL Id: hal-04520815

https://hal.science/hal-04520815v1

Submitted on 26 Mar 2024

HAL is a multi-disciplinary open access
archive for the deposit and dissemination of sci-
entific research documents, whether they are pub-
lished or not. The documents may come from
teaching and research institutions in France or
abroad, or from public or private research centers.

L'archive ouverte pluridisciplinaire HAL, est
destinée au dépôt et à la diffusion de documents
scientifiques de niveau recherche, publiés ou non,
émanant des établissements d'enseignement et de
recherche français ou étrangers, des laboratoires
publics ou privés.

<figure><img src="image_2.png" /></figure>
<figure><img src="image_3.png" /></figure>

# Transient fertilization of a post-Sturtian Snowball ocean margin with dissolved phosphate by clay minerals

Received: 3 August 2023

Accepted: 5 December 2023

Published online: 18 December 2023

<figure><img src="image_4.png" /></figure>

Check for updates

Ernest Chi Fru Ⓓ1, Jalila Al Bahri<fnref n="1" />, Christophe Brosson<fnref n="1" />, Olabode Bankole², Jérémie Aubineau Ⓓ3, Abderrazzak El Albani², Alexandra Nederbragt<fnref n="1" />, Anthony Oldroyd<fnref n="1" />, Alasdair Skelton Ⓓ4, Linda Lowhagen⁴, David Webster⁴, Wilson Y. Fantong⁵, Benjamin J. W. Mills Ⓓ6, Lewis J. Alcott⁶, Kurt O. Konhauser Ⓓ7 & Timothy W. Lyons⁸

Marine sedimentary rocks deposited across the Neoproterozoic Cryogenian Snowball interval, ~720-635 million years ago, suggest that post-Snowball fertilization of shallow continental margin seawater with phosphorus accelerated marine primary productivity, ocean-atmosphere oxygenation, and ultimately the rise of animals. However, the mechanisms that sourced and delivered bioavailable phosphate from land to the ocean are not fully understood. Here we demonstrate a causal relationship between clay mineral production by the melting Sturtian Snowball ice sheets and a short-lived increase in seawater phosphate bioavailability by at least 20-fold and oxygenation of an immediate post-Sturtian Snowball ocean margin. Bulk primary sediment inputs and inferred dissolved seawater phosphate dynamics point to a relatively low marine phosphate inventory that limited marine primary productivity and seawater oxygenation before the Sturtian glaciation, and again in the later stages of the succeeding interglacial greenhouse interval.

The secular rise of phosphorus (P) in Cryogenian marine sediments has been linked to post-Snowball Earth deglaciation resulting in enhanced phosphate (PO₄³⁻) supply to seawater, greater marine primary production, ocean-atmosphere oxygenation, and ultimately the evolution of metazoans<fnref n="1" />⁻³. The inference of higher dissolved seawater PO₄³⁻ concentrations across the Neoproterozoic glaciations comes from Fe-rich deposits and shales containing significantly higher P concentrations relative to older sediments of similar depositional settings<fnref n="1" />,². However, except for a broad association to mechanical weathering caused by erosional action of end-Snowball melting ice sheets, it

remains unclear how PO₄³⁻ was sourced from the continents and transported in quantitatively dissolvable forms to seawater to enable pervasive global ocean-atmosphere oxygenation.

In the modern world, most PO₄³⁻ is transferred from land to the oceans by riverine-transported clay and metal oxide particles rather than in solution⁴⁻⁶. This view is consistent with the suggestion that detrital clay minerals associated with more acidic rivers during the Great Oxygenation Event (GOE) played a significant role in conveying PO₄³⁻ from land to Paleoproterozoic seawater⁵. At times of less acid generation on land, highly reactive iron oxyhydroxides (Fe-oxHR)

<footnote n="1">¹College of Physical and Engineering Sciences, School of Earth and Environmental Sciences, Centre for Geobiology and Geochemistry, Cardiff University, Cardiff CF10 3AT Wales, UK. ²Université de Poitiers UMR 7285-CNRS, Institut de Chimie des Milieux et Matériaux de Poitiers - 5, rue Albert Turpin (Bât B35), 86073 Poitiers, cedex, France. ³Géosciences Environnement Toulouse, CNRS UMR 5563 (CNRS/UPS/IRD/CNES), Université de Toulouse, Observatoire Midi-Pyrénées, Toulouse, France. ⁴Department of Geological Sciences, Stockholm University, 106 91 Stockholm, Sweden. ⁵Institute of Geological and Mining Research (IRGM), Box 4110, Yaoundé, Cameroon. ⁶School of Earth and Environment, University of Leeds, Leeds LS2 9JT, UK. ⁷Department of Earth and Atmospheric Sciences, University of Alberta, Edmonton, Alberta T6G 2E3, Canada. ⁸Department of Earth and Planetary Sciences, University of California, Riverside, CA 92521, USA. ☒e-mail: ChiFruE@Cardiff.ac.uk</footnote>
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# Transient fertilization of a post-Sturtian Snowball ocean margin with dissolved phosphate by clay minerals

Received: 3 August 2023

Accepted: 5 December 2023

Published online: 18 December 2023

<figure><img src="image_4.png" /></figure>

Check for updates

Ernest Chi Fru<sup>1, ∗</sup>, Jalila Al Bahri<sup>1</sup>, Christophe Brosson<sup>1</sup>, Olabode Bankole<sup>2</sup>, Jérémie Aubineau<sup>3</sup>, Abderrazzak El Albani<sup>2</sup>, Alexandra Nederbragt<sup>1</sup>, Anthony Oldroyd<sup>1</sup>, Alasdair Skelton<sup>4</sup>, Linda Lowhagen<sup>4</sup>, David Webster<sup>4</sup>, Wilson Y. Fantong<sup>5</sup>, Benjamin J. W. Mills<sup>6</sup>, Lewis J. Alcott<sup>6</sup>, Kurt O. Konhauser<sup>7</sup> & Timothy W. Lyons<sup>8</sup>

Marine sedimentary rocks deposited across the Neoproterozoic Cryogenian Snowball interval, ~720-635 million years ago, suggest that post-Snowball fertilization of shallow continental margin seawater with phosphorus accelerated marine primary productivity, ocean-atmosphere oxygenation, and ultimately the rise of animals. However, the mechanisms that sourced and delivered bioavailable phosphate from land to the ocean are not fully understood. Here we demonstrate a causal relationship between clay mineral production by the melting Sturtian Snowball ice sheets and a short-lived increase in seawater phosphate bioavailability by at least 20-fold and oxygenation of an immediate post-Sturtian Snowball ocean margin. Bulk primary sediment inputs and inferred dissolved seawater phosphate dynamics point to a relatively low marine phosphate inventory that limited marine primary productivity and seawater oxygenation before the Sturtian glaciation, and again in the later stages of the succeeding interglacial greenhouse interval.

The secular rise of phosphorus (P) in Cryogenian marine sediments has been linked to post-Snowball Earth deglaciation resulting in enhanced phosphate (PO₄³⁻) supply to seawater, greater marine primary production, ocean-atmosphere oxygenation, and ultimately the evolution of metazoans<fnref n="1" />⁻³. The inference of higher dissolved seawater PO₄³⁻ concentrations across the Neoproterozoic glaciations comes from Fe-rich deposits and shales containing significantly higher P concentrations relative to older sediments of similar depositional settings<fnref n="1" />,². However, except for a broad association to mechanical weathering caused by erosional action of end-Snowball melting ice sheets, it

remains unclear how PO₄³⁻ was sourced from the continents and transported in quantitatively dissolvable forms to seawater to enable pervasive global ocean-atmosphere oxygenation.

In the modern world, most PO₄³⁻ is transferred from land to the oceans by riverine-transported clay and metal oxide particles rather than in solution⁴⁻⁶. This view is consistent with the suggestion that detrital clay minerals associated with more acidic rivers during the Great Oxygenation Event (GOE) played a significant role in conveying PO₄³⁻ from land to Paleoproterozoic seawater⁵. At times of less acid generation on land, highly reactive iron oxyhydroxides (Fe-oxHR)

<footnote n="1">¹College of Physical and Engineering Sciences, School of Earth and Environmental Sciences, Centre for Geobiology and Geochemistry, Cardiff University, Cardiff CF10 3AT Wales, UK. ²Université de Poitiers UMR 7285-CNRS, Institut de Chimie des Milieux et Matériaux de Poitiers - 5, rue Albert Turpin (Bât B35), 86073 Poitiers, cedex, France. ³Géosciences Environnement Toulouse, CNRS UMR 5563 (CNRS/UPS/IRD/CNES), Université de Toulouse, Observatoire Midi-Pyrénées, Toulouse, France. ⁴Department of Geological Sciences, Stockholm University, 106 91 Stockholm, Sweden. ⁵Institute of Geological and Mining Research (IRGM), Box 4110, Yaoundé, Cameroon. ⁶School of Earth and Environment, University of Leeds, Leeds LS2 9JT, UK. ⁷Department of Earth and Atmospheric Sciences, University of Alberta, Edmonton, Alberta T6G 2E3, Canada. ⁸Department of Earth and Planetary Sciences, University of California, Riverside, CA 92521, USA. ☑ e-mail: ChiFruE@Cardiff.ac.uk</footnote>
instead served as efficient particulate sorbents for dissolved phosphate⁵. As a corollary, we hypothesize that extensive weathering of continental landmasses by melting ice sheets at the end of the Cryogenian Snowball Earth glaciations⁷ drove up production, transport, and supply of fine-grained detrital clays and Fe-oxHR to the oceans, which served as vectors of marginal seawater enrichment with PO₄³⁻. Indeed, melting of the modern Greenland ice sheet shows that up to 97% PO₄³⁻ exported by glacial meltwater is associated with suspended sediment particles⁸. This relationship is predictable, given that clay minerals, which tend to form rapidly upon the retreat of glaciers with climate warming⁹, together with Fe-oxHR, possess large surface-to-volume ratios. Together, they contain positive charged surfaces at the pH range of rivers that make them efficient adsorbents of dissolved PO₄³⁻ anions⁴⁻⁶,¹⁰⁻¹⁷.

To assess the potential of clay minerals and Fe-oxHR minerals as vectors of dissolved PO₄³⁻ to post-Snowball seawater, we collected marine sediments exposed on the Isles of Islay and the Garvellachs in the Dalradian Supergroup, Scotland, spanning pre-glacial, deglacial, and post-glacial phases of the Neoproterozoic Sturtian Snowball glaciation⁷ (Fig. 1). The underlying pre-Snowball Tonian Lossit Limestone Formation (LLF) in the >4-km-thick Appin Group¹⁸⁻²³ is characterized by organic-rich mudstones, sandstones, carbonate, and shallow seawater stromatolites. The glaciogenic tillite cap of the LLF passes conformably²¹ into the overlying ~1.1 km-thick Port Askraig Tillite Formation (PATF), correlated worldwide to Sturtian Snowball deposits based on geochronology, lithostratigraphy, and chemostratigraphy¹⁸⁻²³. On the Garvellachs Island, the PATF appears as

twelve discrete diamictite units containing dolostone clasts overlain by the ~40-m-thick Great Breccia, comprised of deformed sediment bedrock rafts transported by icebergs from land to the ocean margin, and the 29 to 40-m-thick disrupted beds dominated by Fe-rich siltstones and dolostone concretions. Up-section, ~30 diamictite layers with interlayered sandstone units grade upwards into transported granitic clasts, which are in turn conformably overlain by the post-Snowball Bonahaven Dolomite Formation¹⁸,¹⁹,²¹ (BDF). The BDF consists of ~300-m-thick fine-grained clastic rocks composed of siltstones and mudstones, with occasional stromatolitic dolostone and evaporitic deposits indicating deposition in arid greenhouse climate times¹⁸⁻²³.

In this study, we use a combination of geochemical techniques to demonstrate a causal relationship between continental erosion and the supply of dissolved PO₄³⁻ to continental margin waters and associated temporal controls on seawater oxygenation dynamics across the Sturtian Snowball glaciation deposits of the Dalradian Supergroup.

## Results and discussion

### Bulk facies chemostratigraphy and mineralogy

Careful collection of outcrop samples took place in the field to avoid weathered and metamorphosed lithologies (Table S1). Comparative chemostratigraphic correlation of bulk facies geochemistry and δ¹³Ccarbonate and δ¹⁸Ocarbonate compositions (Figs. 2 & S1-S2) with previous studies of the same section¹⁸⁻²⁴, together with sediment mineralogy (Fig. 3 & Table S2), was used to evaluate data quality and to account for potential post-depositional alteration of primary geochemical composition. In addition, cross plots of Fe/Ti vs.

<figure><img src="image_5.png" /><figcaption>**Fig. 1 |** Study locality, lithology, and stratigraphy. a Geological map and lithology of the sampled sections. The black rectangular box in the green map, enlarged to scale to the left, displays the spatial distribution and location of sampled outcrops.</figcaption></figure>

b Stratigraphy and ages within the Dalradian Supergroup of sampled outcrops boxed in red. LLF Lossit Limestone Formation, PATF Port Askraig Tillite Formation, BDF Bonahaven Dolomite Formation.
instead served as efficient particulate sorbents for dissolved phosphate⁵. As a corollary, we hypothesize that extensive weathering of continental landmasses by melting ice sheets at the end of the Cryogenian Snowball Earth glaciations⁷ drove up production, transport, and supply of fine-grained detrital clays and Fe-oxHR to the oceans, which served as vectors of marginal seawater enrichment with PO₄³⁻. Indeed, melting of the modern Greenland ice sheet shows that up to 97% PO₄³⁻ exported by glacial meltwater is associated with suspended sediment particles⁸. This relationship is predictable, given that clay minerals, which tend to form rapidly upon the retreat of glaciers with climate warming⁹, together with Fe-oxHR, possess large surface-to-volume ratios. Together, they contain positive charged surfaces at the pH range of rivers that make them efficient adsorbents of dissolved PO₄³⁻ anions⁴⁻⁶,¹⁰⁻¹⁷.

To assess the potential of clay minerals and Fe-oxHR minerals as vectors of dissolved PO₄³⁻ to post-Snowball seawater, we collected marine sediments exposed on the Isles of Islay and the Garvellachs in the Dalradian Supergroup, Scotland, spanning pre-glacial, deglacial, and post-glacial phases of the Neoproterozoic Sturtian Snowball glaciation⁷ (Fig. 1). The underlying pre-Snowball Tonian Lossit Limestone Formation (LLF) in the >4-km-thick Appin Group¹⁸⁻²³ is characterized by organic-rich mudstones, sandstones, carbonate, and shallow seawater stromatolites. The glaciogenic tillite cap of the LLF passes conformably²¹ into the overlying ~1.1 km-thick Port Askraig Tillite Formation (PATF), correlated worldwide to Sturtian Snowball deposits based on geochronology, lithostratigraphy, and chemostratigraphy¹⁸⁻²³. On the Garvellachs Island, the PATF appears as

twelve discrete diamictite units containing dolostone clasts overlain by the ~40-m-thick Great Breccia, comprised of deformed sediment bedrock rafts transported by icebergs from land to the ocean margin, and the 29 to 40-m-thick disrupted beds dominated by Fe-rich siltstones and dolostone concretions. Up-section, ~30 diamictite layers with interlayered sandstone units grade upwards into transported granitic clasts, which are in turn conformably overlain by the post-Snowball Bonahaven Dolomite Formation¹⁸,¹⁹,²¹ (BDF). The BDF consists of ~300-m-thick fine-grained clastic rocks composed of siltstones and mudstones, with occasional stromatolitic dolostone and evaporitic deposits indicating deposition in arid greenhouse climate times¹⁸⁻²³.

In this study, we use a combination of geochemical techniques to demonstrate a causal relationship between continental erosion and the supply of dissolved PO₄³⁻ to continental margin waters and associated temporal controls on seawater oxygenation dynamics across the Sturtian Snowball glaciation deposits of the Dalradian Supergroup.

## Results and discussion

### Bulk facies chemostratigraphy and mineralogy

Careful collection of outcrop samples took place in the field to avoid weathered and metamorphosed lithologies (Table S1). Comparative chemostratigraphic correlation of bulk facies geochemistry and δ¹³Ccarbonate and δ¹⁸Ocarbonate compositions (Figs. 2 & S1-S2) with previous studies of the same section¹⁸⁻²⁴, together with sediment mineralogy (Fig. 3 & Table S2), was used to evaluate data quality and to account for potential post-depositional alteration of primary geochemical composition. In addition, cross plots of Fe/Ti vs.

<figure><img src="image_5.png" /><figcaption>**Fig. 1** | **Study locality, lithology, and stratigraphy.** a Geological map and lithology of the sampled sections. The black rectangular box in the green map, enlarged to scale to the left, displays the spatial distribution and location of sampled outcrops.</figcaption></figure>

b Stratigraphy and ages within the Dalradian Supergroup of sampled outcrops boxed in red. LLF Lossit Limestone Formation, PATF Port Askraig Tillite Formation, BDF Bonahaven Dolomite Formation.
<figure><img src="image_6.png" /><figcaption>**Fig. 2** | Box and whisker plots showing lithostratigraphic carbon systematics for representative samples. a $\delta^{13}C_{\text{org}}$ distribution. b Organic carbon ($C_{\text{org}}$) concentration. c $\delta^{13}C_{\text{carbonate}}$ distribution. d Carbonate concentration. e $\delta^{18}O_{\text{carbonates}}$ distribution.</figcaption></figure>

Centre line = median value; whiskers = minimum and maximum values; dots = outliers; box limits = lower and upper quartiles.

<figure><img src="image_7.png" /><figcaption>**Fig. 3** | Examples of Scanning Electron Microscopy-Energy Dispersive Spectroscopy (SEM-EDS) maps and bulk XRD mineralogical patterns for representative samples. a, b SEM-EDS mineral maps for immediate post-Snowball, composed of fine-grain siliciclastic sediments. c Corresponding immediate post-Snowball whole rock XRD mineral diffractogram. d Representative SEM-EDS mineral map for Post Askaig tillite showing coarse siliciclastic grains dominated by</figcaption></figure>

fine orange muscovite phyllosilicate (sheet silicate) grains. e Corresponding XRD mineral diffractogram for the Port Askaig Tillites. f An example of an SEM-EDS mineral map for a pre-Snowball sample from the LLF, showing coarse siliciclastic grains, but with much lower phyllosilicate silicate content compared to the tillites. g Corresponding immediate pre-Snowball whole rock XRD mineral diffractogram.

Al/(Al+Fe+Mn) (ref. 25) were used to constrain the potential influence of hydrothermal fluids (Fig. S3). Our $\delta^{13}C_{\text{carbonate}}$ and $\delta^{18}O_{\text{carbonate}}$ values fall within the range reported in previous studies for the pre-glacial, glacial and post-glacial lithologies$^{18,19,21-23}$, which have been correlated by geochronology and chemo/lithostratigraphy to the Cryogenian-Sturtian interval in Australia, Mongolia, Siberia, China, Oman, Namibia and Canada$^{7,18,19}$. The pre-/late-Snowball samples are marked by higher $\delta^{13}C_{\text{org}}$, $C_{\text{org}}$ and $\delta^{13}C_{\text{carbonate}}$ excursions, compared to persistently lower tillite and immediate post-Snowball values (Fig. 2a-c). Although characterized by lower carbonate content relative to concentrations in tillite samples analyzed for C isotope distribution (Fig. 2d), X-ray diffraction (XRD) and thin-sectioned Scanning Electron Microscopy-Energy Dispersive Spectroscopy (SEM-EDS) data are

consistent with reported higher and more homogenous carbonate enrichment in the pre-/late-Snowball facies$^{18,19,21,22}$ (Fig. 3 & Table S2). Associated $\delta^{18}O_{\text{carbonate}}$ trends generally decline up sequence (Fig. 2e), while the absence of $\delta^{13}C$ and $\delta^{18}O$ correlation suggests negligible diagenetic alteration of primary $\delta^{13}C_{\text{carbonate}}$ signal (Fig. S2).

Lithologies affected by greenschist metamorphism, confined to the margins of metabasaltic sills$^{24}$, were excluded. Consistent with this sampling strategy, XRD and thin-sectioned SEM-EDS mineralogical analysis, revealed a major dominance of no to low-grade metamorphic clay minerals (Fig. 3 & Table S2). Typical clay minerals like kaolinite that are often associated with strong terrestrial weathering by chemical processes are rare in the samples, while muscovite and illite clay minerals believed to be most abundant in the modern
<figure><img src="image_6.png" /><figcaption>**Fig. 2** | Box and whisker plots showing lithostratigraphic carbon systematics for representative samples. **a** $\delta^{13}C_{\text{org}}$ distribution. **b** Organic carbon ($C_{\text{org}}$) concentration. **c** $\delta^{13}C_{\text{carbonate}}$ distribution. **d** Carbonate concentration. **e** $\delta^{18}O_{\text{carbonates}}$ distribution.</figcaption></figure>

Centre line = median value; whiskers = minimum and maximum values; dots = outliers; box limits = lower and upper quartiles.

<figure><img src="image_7.png" /><figcaption>**Fig. 3** | Examples of Scanning Electron Microscopy-Energy Dispersive Spectroscopy (SEM-EDS) maps and bulk XRD mineralogical patterns for representative samples. **a**, **b** SEM-EDS mineral maps for immediate post-Snowball, composed of fine-grain siliciclastic sediments. **c** Corresponding immediate post-Snowball whole rock XRD mineral diffractogram. **d** Representative SEM-EDS mineral map for Post Askaig tillite showing coarse siliciclastic grains dominated by</figcaption></figure>

fine orange muscovite phyllosilicate (sheet silicate) grains. **e** Corresponding XRD mineral diffractogram for the Port Askaig Tillites. **f** An example of an SEM-EDS mineral map for a pre-Snowball sample from the LLF, showing coarse siliciclastic grains, but with much lower phyllosilicate silicate content compared to the tillites. **g** Corresponding immediate pre-Snowball whole rock XRD mineral diffractogram.

$\text{Al/(Al+Fe+Mn)}$ (ref. 25) were used to constrain the potential influence of hydrothermal fluids (Fig. S3). Our $\delta^{13}C_{\text{carbonate}}$ and $\delta^{18}O_{\text{carbonate}}$ values fall within the range reported in previous studies for the pre-glacial, glacial and post-glacial lithologies$^{18,19,21-23}$, which have been correlated by geochronology and chemo/lithostratigraphy to the Cryogenian-Sturtian interval in Australia, Mongolia, Siberia, China, Oman, Namibia and Canada$^{7,18,19}$. The pre-/late-Snowball samples are marked by higher $\delta^{13}C_{\text{org}}$, $C_{\text{org}}$ and $\delta^{13}C_{\text{carbonate}}$ excursions, compared to persistently lower tillite and immediate post-Snowball values (Fig. 2a-c). Although characterized by lower carbonate content relative to concentrations in tillite samples analyzed for C isotope distribution (Fig. 2d), X-ray diffraction (XRD) and thin-sectioned Scanning Electron Microscopy-Energy Dispersive Spectroscopy (SEM-EDS) data are

consistent with reported higher and more homogenous carbonate enrichment in the pre-/late-Snowball facies$^{18,19,21,22}$ (Fig. 3 & Table S2). Associated $\delta^{18}O_{\text{carbonate}}$ trends generally decline up sequence (Fig. 2e), while the absence of $\delta^{13}C$ and $\delta^{18}O$ correlation suggests negligible diagenetic alteration of primary $\delta^{13}C_{\text{carbonate}}$ signal (Fig. S2).

Lithologies affected by greenschist metamorphism, confined to the margins of metabasaltic sills$^{24}$, were excluded. Consistent with this sampling strategy, XRD and thin-sectioned SEM-EDS mineralogical analysis, revealed a major dominance of no to low-grade metamorphic clay minerals (Fig. 3 & Table S2). Typical clay minerals like kaolinite that are often associated with strong terrestrial weathering by chemical processes are rare in the samples, while muscovite and illite clay minerals believed to be most abundant in the modern
<figure><img src="image_8.png" /><figcaption>**Fig. 4** | Major and trace element distribution and lost on ignition (LOI) trends across the sampled sequence. a-e Major element distribution. f-i Trace metal distribution. j-q Major and trace metal composition normalized to TiO₂. r LOI trend. s-y Trace element enrichment factors (EF), calculated as EFₓ = [(X/Al)ₙₙₐₙ/ (X/Al)ₙₐₙ], where X = concentration of element of interest according to Tribovillard and others (ref. 73). UCC, upper continental crust reference values</figcaption></figure>

according to Rudnick and Gao (ref. 74). LLF, Lossit Limestone Formation. PATF, Port Askaig Tillites. PAT, Port Askaig Tillites, where PAT1 and PAT2 represent tillites from the Port Askaig type location on Islay and PAT3 to PAT5 the LL-16-a sample at the top of the LLF that conformably underlines the Port Askaig tillites. BDF, Bonahaven Dolomite Formation. Major and trace element enrichment patterns.

upper continental crust (UCC)¹⁷, occur more commonly across the lithofacies (Fig. 3 & Table S2). Chlorite, which also tends to be enriched in the UCC, was detected mainly in the deglaciating tillites, while the presence of albite (a tectosilicate mineral) in all samples regardless of lithology (Fig. 3), suggests an association with the erosion of crystalline bedrocks¹⁹.

Overall, the SEM-EDS mineral maps together with XRD mineralogical analysis, show a variable prevalence of siliciclastic detrital material in all lithologies, with a dominance of sheet silicates and quartz, even in carbonate-rich facies. These findings agree with past observations¹⁸⁻²³, evidenced here by fine-grained siliciclastic particles in post-Snowball sediments and the prevalence of coarser quartz grains in tillite and pre-Snowball samples. The tillites are noted for hosting abundant detrital grains likely associated with illite, muscovite, albite, and, to a lesser extent, kaolinite (Fig. 3d-e & Table 2S). Illite and muscovite are quantitatively more abundant in the post-Snowball facies. Although detected in the pre-Snowball rocks, illite is not always present in readily quantifiable amounts. Typically, chemical weathering of most rock-forming silicates promotes secondary formation of clay minerals and Fe(III)- and Al-oxides, with an accumulation of residual quartz, heavy minerals, and sheet silicates like muscovite and biotite²⁶. Sediments and soils originating from this process can predictably contain >50% sheet silicates and Fe oxyhydroxides by volume, depending on the nature of the source rocks and prevailing climatic conditions¹⁷,²⁶. The variable occurrence of illite and muscovite across all sampled lithologies could be due to varying degrees of detrital supply or distinct local diagenetic pathways, while the largely low kaolinite content may be the result of possible transformation because kaolinite reacts with K-feldspar to form illite during burial diagenesis¹⁷ and with alkaline fluids during metasomatism. Although chlorite can also form as a low-grade metamorphic mineral, with further transformation to muscovite at higher temperatures, the mineralogy of the facies is consistent with their suggested low metamorphic grade and observed preservation of primary features¹⁸⁻²³. Further, the notable prevalence of quartz and sheet silicates (mainly clay minerals), including co-occurrence with tectosilicate albite, hint at the dominant

supply of clastic debris to the primary sediments, derived from physical erosion of intermediate-to-felsic continental rocks (Fig. S4).

## Bulk sediment geochemistry

A wide range of geochemical changes emerge along the studied lithostatigraphic section (Fig. 4 & Table S3), distinguished by persistently elevated bulk sediment P₂O₅, TiO₂, Al₂O₃, Fe₂O₃, Cr, V, and Ni concentrations in the PATF and the lower BDF, with much lower and more variable concentrations recorded in the PS-16 section of the Port an t-Struthain rocks in the upper BDF (Fig. 4a-c & f-h). Notable Al₂O₃ and TiO₂ peaks, especially in the PATF and lower BDF, agree with the prevalence of various mineral phases pointing to substantial detrital contribution to sediment accumulation across the sequence. To test this idea, elemental normalization to Ti—a detrital indicator of authigenic enrichment²⁷,²⁸—shows subtle enrichment consisting of two broad patterns across the stratigraphic profile (Fig. 4j-p). This relationship is highlighted by two observations. First, a reasonable stratigraphic correlation exists between P/Ti and Fe/Ti and to some degree with Mn/Ti ratios (Fig. 4n-p), although generally, MnO does not show significant lithostatigraphic variations (Fig. 4d). Second, a broad minimal correlation is observed for Cr/Ti, V/Ti, Ni/Ti, and Co/Ti (Fig. 4j-m), suggesting that their accumulation was co-regulated by the same sedimentary processes.

Interestingly, Cr/Ti is anomalous in the sense that in the lower BDF, when the other elements display multiple peaks, Cr/Ti distribution remains uniform, but becomes noticeable when enrichment in most elements is muted in the upper BDF. Port an t-Struthain section (i.e., the PS-16 samples). To add to these observations, the near static Al₂O₃ to TiO₂ ratios (Fig. 4q) are interpreted to either reflect stable detrital contribution and/or potential long-term sediment accumulation from a similar UCC rock source.

Comparable Fe₂O₃ to TiO₂ and P₂O₅ to TiO₂ ratios, together with Loss on Ignition (LOI) being inversely correlated with P₂O₅ and Fe₂O₃ content throughout the sampled section (Fig. 4r & Fig. S5), suggest bulk sediment P₂O₅ and Fe₂O₃ are most likely preserved in inorganic instead of organic and carbonate mineral phases. Where LOI values are elevated, they presumably predict higher combustible sedimentary
<figure><img src="image_8.png" /><figcaption>**Fig. 4** | Major and trace element distribution and lost on ignition (LOI) trends across the sampled sequence. a-e Major element distribution. f-i Trace metal distribution. j-q Major and trace metal composition normalized to TiO₂. r LOI trend. s-y Trace element enrichment factors (EF), calculated as EFₓ = [(X/Al)ₙₙₐₙ/ (X/Al)ₙₐₙ], where X = concentration of element of interest according to Tribovillard and others (ref. 73). UCC, upper continental crust reference values</figcaption></figure>

according to Rudnick and Gao (ref. 74). LLF, Lossit Limestone Formation. PATF, Port Askaig Tillites. PAT, Port Askaig Tillites, where PAT1 and PAT2 represent tillites from the Port Askaig type location on Islay and PAT3 to PAT5 the LL-16-a sample at the top of the LLF that conformably underlines the Port Askaig tillites. BDF, Bonahaven Dolomite Formation. Major and trace element enrichment patterns.

upper continental crust (UCC)¹⁷, occur more commonly across the lithofacies (Fig. 3 & Table S2). Chlorite, which also tends to be enriched in the UCC, was detected mainly in the deglaciating tillites, while the presence of albite (a tectosilicate mineral) in all samples regardless of lithology (Fig. 3), suggests an association with the erosion of crystalline bedrocks¹⁹.

Overall, the SEM-EDS mineral maps together with XRD mineralogical analysis, show a variable prevalence of siliciclastic detrital material in all lithologies, with a dominance of sheet silicates and quartz, even in carbonate-rich facies. These findings agree with past observations¹⁸⁻²³, evidenced here by fine-grained siliciclastic particles in post-Snowball sediments and the prevalence of coarser quartz grains in tillite and pre-Snowball samples. The tillites are noted for hosting abundant detrital grains likely associated with illite, muscovite, albite, and, to a lesser extent, kaolinite (Fig. 3d-e & Table 2S). Illite and muscovite are quantitatively more abundant in the post-Snowball facies. Although detected in the pre-Snowball rocks, illite is not always present in readily quantifiable amounts. Typically, chemical weathering of most rock-forming silicates promotes secondary formation of clay minerals and Fe(III)- and Al-oxides, with an accumulation of residual quartz, heavy minerals, and sheet silicates like muscovite and biotite²⁶. Sediments and soils originating from this process can predictably contain >50% sheet silicates and Fe oxyhydroxides by volume, depending on the nature of the source rocks and prevailing climatic conditions¹⁷,²⁶. The variable occurrence of illite and muscovite across all sampled lithologies could be due to varying degrees of detrital supply or distinct local diagenetic pathways, while the largely low kaolinite content may be the result of possible transformation because kaolinite reacts with K-feldspar to form illite during burial diagenesis¹⁷ and with alkaline fluids during metasomatism. Although chlorite can also form as a low-grade metamorphic mineral, with further transformation to muscovite at higher temperatures, the mineralogy of the facies is consistent with their suggested low metamorphic grade and observed preservation of primary features¹⁸⁻²³. Further, the notable prevalence of quartz and sheet silicates (mainly clay minerals), including co-occurrence with tectosilicate albite, hint at the dominant

supply of clastic debris to the primary sediments, derived from physical erosion of intermediate-to-felsic continental rocks (Fig. S4).

## Bulk sediment geochemistry

A wide range of geochemical changes emerge along the studied lithostatigraphic section (Fig. 4 & Table S3), distinguished by persistently elevated bulk sediment P₂O₅, TiO₂, Al₂O₃, Fe₂O₃, Cr, V, and Ni concentrations in the PATF and the lower BDF, with much lower and more variable concentrations recorded in the PS-16 section of the Port an t-Struthain rocks in the upper BDF (Fig. 4a-c & f-h). Notable Al₂O₃ and TiO₂ peaks, especially in the PATF and lower BDF, agree with the prevalence of various mineral phases pointing to substantial detrital contribution to sediment accumulation across the sequence. To test this idea, elemental normalization to Ti—a detrital indicator of authigenic enrichment²⁷,²⁸—shows subtle enrichment consisting of two broad patterns across the stratigraphic profile (Fig. 4j-p). This relationship is highlighted by two observations. First, a reasonable stratigraphic correlation exists between P/Ti and Fe/Ti and to some degree with Mn/Ti ratios (Fig. 4n-p), although generally, MnO does not show significant lithostatigraphic variations (Fig. 4d). Second, a broad minimal correlation is observed for Cr/Ti, V/Ti, Ni/Ti, and Co/Ti (Fig. 4j-m), suggesting that their accumulation was co-regulated by the same sedimentary processes.

Interestingly, Cr/Ti is anomalous in the sense that in the lower BDF, when the other elements display multiple peaks, Cr/Ti distribution remains uniform, but becomes noticeable when enrichment in most elements is muted in the upper BDF. Port an t-Struthain section (i.e., the PS-16 samples). To add to these observations, the near static Al₂O₃ to TiO₂ ratios (Fig. 4q) are interpreted to either reflect stable detrital contribution and/or potential long-term sediment accumulation from a similar UCC rock source.

Comparable Fe₂O₃ to TiO₂ and P₂O₅ to TiO₂ ratios, together with Loss on Ignition (LOI) being inversely correlated with P₂O₅ and Fe₂O₃ content throughout the sampled section (Fig. 4r & Fig. S5), suggest bulk sediment P₂O₅ and Fe₂O₃ are most likely preserved in inorganic instead of organic and carbonate mineral phases. Where LOI values are elevated, they presumably predict higher combustible sedimentary
<figure><img src="image_9.png" /></figure>

<figure><img src="image_10.png" /></figure>

<figure><img src="image_11.png" /><figcaption>**Fig. 5** | Major trace elements cross plots for pre-Snowball (LLF), Tillites (PATF) and post-Snowball (BDF). **a** P₂O₅ versus Fe₂O₃, **b** P₂O₅ versus TiO₂, **c** P₂O₅ versus Al₂O₃, **d** Fe₂O₃ versus TiO₂, **e** Fe₂O₃ versus Al₂O₃, **f** Al₂O₃ versus TiO₂. LLF, Lossit</figcaption></figure>

<figure><img src="image_12.png" /></figure>

<figure><img src="image_13.png" /></figure>

<figure><img src="image_14.png" /></figure>

Limestone Formation. PATF, Port Askaig Tillites. BDF, Bonahaven Dolomite Formation.

organic and/or carbonate content, while lower values indicate the
contrary, due to higher susceptibility of carbonates and organic matter
to complete combustion to CO₂ under elevated temperatures²⁹.
Indeed, the lowest LOI values are recorded in the carbonate-poor PATF
and lower BDF section where sustained peak P₂O₅ and Fe₂O₃ con-
centrations are found, compared to the minor and more variable P₂O₅
content in the carbonate-rich LLF and upper BDF PS-16 facies (Figs. 4c,
e & 3r). Higher LOI values that tend to relate inversely with P₂O₅ and
Fe₂O₃ concentrations across the section (Fig. S5), are unique to the
carbonate-rich LLF and PS-16 upper BDF samples. Measured trace
metals are generally enriched across the sequence relative to UCC
values (Fig. 4s-y). Notably, significant co-enrichment of P is also
observed in the tillites and upwards relative to the UCC, compared to
pre-Snowball times (Fig. 4t). Despite their overall similar redox prop-
erties, Mn enrichment patterns relative to the UCC are dissimilar to
those of Fe, particularly in some tillite and immediate post-Snowball
samples (Fig. 4s & u), pointing perhaps to different enrichment

pathways or the known differences in sensitivity to reduction. Chrom-
mium shows two anomalous enrichment peaks relative to UCC, one in
the LLF that is also seen for V and Fe and a second corresponding to
samples shown above to have high Cr/Ti ratios in the upper BDF
(Fig. 4j, s, x & y).

The generally low C<sub>org</sub> levels across the sampled sequence (Fig. 2b) are considered to be of little importance to sedimentary P and Fe preservation. Positive correlations are revealed for P<sub>2</sub>O<sub>5</sub> and Fe<sub>2</sub>O<sub>3</sub> and poorly mobile TiO<sub>2</sub> and Al<sub>2</sub>O<sub>3</sub> across lithostratigraphy, although they are much weaker with respect to Al<sub>2</sub>O<sub>3</sub> for the pre-Snowball Earth LLF samples (Fig. 5a-c). A similar relation appears for Fe<sub>2</sub>O<sub>3</sub> versus TiO<sub>2</sub> and Al<sub>2</sub>O<sub>3</sub> plots, but like P<sub>2</sub>O<sub>5</sub> the correlation is unsupported for Al<sub>2</sub>O<sub>3</sub> in the LLF section (Fig. 5d-e). When considered in light of the strong positive correlation between Al<sub>2</sub>O<sub>3</sub> and TiO<sub>2</sub> (Fig. 5f) and Fe<sub>2</sub>O<sub>3</sub> and P<sub>2</sub>O<sub>5</sub> (Fig. 5a) in all three lithological sections, the observations suggest some level of decoupling of pre-Snowball P<sub>2</sub>O<sub>5</sub> and Fe<sub>2</sub>O<sub>3</sub> enrichment pathways with respect to Al<sub>2</sub>O<sub>3</sub> sources (Fig. 5d-f). The strong
<figure><img src="image_9.png" /></figure>

<figure><img src="image_10.png" /></figure>

<figure><img src="image_11.png" /><figcaption>**Fig. 5** | Major trace elements cross plots for pre-Snowball (LLF), Tillites (PATF) and post-Snowball (BDF). **a** P₂O₅ versus Fe₂O₃, **b** P₂O₅ versus TiO₂, **c** P₂O₅ versus Al₂O₃, **d** Fe₂O₃ versus TiO₂, **e** Fe₂O₃ versus Al₂O₃, **f** Al₂O₃ versus TiO₂. LLF, Lossit</figcaption></figure>

<figure><img src="image_12.png" /></figure>

<figure><img src="image_13.png" /></figure>

<figure><img src="image_14.png" /></figure>

Limestone Formation. PATF, Port Askaig Tillites. BDF, Bonahaven Dolomite Formation.

organic and/or carbonate content, while lower values indicate the
contrary, due to higher susceptibility of carbonates and organic matter
to complete combustion to CO₂ under elevated temperatures²⁹.
Indeed, the lowest LOI values are recorded in the carbonate-poor PATF
and lower BDF section where sustained peak P₂O₅ and Fe₂O₃ con-
centrations are found, compared to the minor and more variable P₂O₅
content in the carbonate-rich LLF and upper BDF PS-16 facies (Figs. 4c,
e & 3r). Higher LOI values that tend to relate inversely with P₂O₅ and
Fe₂O₃ concentrations across the section (Fig. S5), are unique to the
carbonate-rich LLF and PS-16 upper BDF samples. Measured trace
metals are generally enriched across the sequence relative to UCC
values (Fig. 4s-y). Notably, significant co-enrichment of P is also
observed in the tillites and upwards relative to the UCC, compared to
pre-Snowball times (Fig. 4t). Despite their overall similar redox prop-
erties, Mn enrichment patterns relative to the UCC are dissimilar to
those of Fe, particularly in some tillite and immediate post-Snowball
samples (Fig. 4s & u), pointing perhaps to different enrichment

pathways or the known differences in sensitivity to reduction. Chrom-
mium shows two anomalous enrichment peaks relative to UCC, one in
the LLF that is also seen for V and Fe and a second corresponding to
samples shown above to have high Cr/Ti ratios in the upper BDF
(Fig. 4j, s, x & y).

The generally low C<sub>org</sub> levels across the sampled sequence (Fig. 2b) are considered to be of little importance to sedimentary P and Fe preservation. Positive correlations are revealed for P<sub>2</sub>O<sub>5</sub> and Fe<sub>2</sub>O<sub>3</sub> and poorly mobile TiO<sub>2</sub> and Al<sub>2</sub>O<sub>3</sub> across lithostratigraphy, although they are much weaker with respect to Al<sub>2</sub>O<sub>3</sub> for the pre-Snowball Earth LLF samples (Fig. 5a-c). A similar relation appears for Fe<sub>2</sub>O<sub>3</sub> versus TiO<sub>2</sub> and Al<sub>2</sub>O<sub>3</sub> plots, but like P<sub>2</sub>O<sub>5</sub> the correlation is unsupported for Al<sub>2</sub>O<sub>3</sub> in the LLF section (Fig. 5d-e). When considered in light of the strong positive correlation between Al<sub>2</sub>O<sub>3</sub> and TiO<sub>2</sub> (Fig. 5f) and Fe<sub>2</sub>O<sub>3</sub> and P<sub>2</sub>O<sub>5</sub> (Fig. 5a) in all three lithological sections, the observations suggest some level of decoupling of pre-Snowball P<sub>2</sub>O<sub>5</sub> and Fe<sub>2</sub>O<sub>3</sub> enrichment pathways with respect to Al<sub>2</sub>O<sub>3</sub> sources (Fig. 5d-f). The strong
correlations between TiO₂, P₂O₅ and Fe₂O₃ for tillites and post-Snowball facies may consequently be the result of sediment source homogenization by the indiscriminate erosional action of melting ice sheets. Regardless, these observations provide further evidence for across sequence P₂O₅ and Fe₂O₃ enrichment by detritus.

The low C<sub>org</sub> and negative δ<sup>13</sup>C<sub>carbonate</sub> distribution in the facies (Fig. 2 & S1-S2) suggest microbial oxidation of C<sub>org</sub> likely prevailed at the sediment-water interface, which would have promoted the release of organic-bound P into sea and sediment pore water, influencing dissolved aqueous P content and eventual incorporation into various sedimentary minerals. This would have been particularly relevant in the immediate post-Snowball interval where apatite formation became more pronounced, compared to the rest of the section (Fig. 3 & Table S2). It is also possible that prevailing environmental conditions influenced ongoing microbial transformation of P-rich C<sub>org</sub> and Fe-ox<sub>HR</sub> minerals to trigger enough diagenetic sediment porewater P supersaturation<sup>30</sup>. For example, the geochemical data suggest that bulk primary sediment P was predominantly associated with non-calcium bearing minerals such as Fe-ox<sub>HR</sub> and unreactive detrital silicate phases (Figs. S6-S9), which would have starved primary sediments of dissolved P. Except for some immediate post-Snowball samples, across-sequence CaO and P₂O₅ inverse correlations, being up to 79% for the tillites (Fig. S6a-b), corroborate limited potential P preservation in non-calcium bearing mineral phases. As discussed above, this view is supported by low LOI, low-carbonate facies associated with bulk high P₂O₅/Fe₂O₃ ratios and high LOI, high-carbonate lithologies with bulk low-P₂O₅/Fe₂O₃ ratios (Fig. S5). Overall decreasing P₂O₅ concentration coincides with C<sub>org</sub> content that increases from post-Snowball to pre-Snowball facies (Fig. S6c), signalling either possible diagenetic P enrichment or loss in primary sediments through microbial oxidation of organic-rich P biomass originating from the water column. Indeed, our lowest δ<sup>13</sup>C<sub>org</sub> and C<sub>org</sub> values in the tillites and immediate post-Snowball interval (Fig. 2a-b) coincide with P₂O₅ enrichment compared to the low P₂O₅ pre-Snowball samples (Fig. S6c-d). Based on these observations, microbial recycling of organic-rich P at the sediment-water interface could explain the increasing prevalence of apatite in the immediate post-Snowball interval. However, the data suggest that the P supersaturation required to spontaneously precipitate large amounts of apatite precursor phases and significant substitution in carbonate minerals<sup>30,31</sup> was limited, especially in the pre-Snowball interval. Instead, our results indicate that dominant P supply and enrichment in the primary sediments mostly reflect detrital loading with non-apatite minerals. Moreover, as we show below, the synthesis of Ca-rich P minerals was perhaps limited by abundant Fe-ox<sub>HR</sub> particles acting as efficient scavengers of dissolved PO₄³⁻ at the sediment seawater interface.

Redox-sensitive Mn shows a weak negative correlation with TiO₂ and Al₂O₃ across all facies (Fig. S10), suggesting that Mn enrichment pathways are to some extent decoupled from those of P₂O₅ and Fe₂O₃, particularly given the considerable positive correlation between P₂O₅, TiO₂, and Al₂O₃ (Fig. 5). Except for the short-lived spike in Cr enrichment in the upper BDF relative to Ti, overall, our data do not indicate that significant oxidative/chemical weathering of terrestrial rocks was a predominant mechanism for PO₄³⁻ delivery to seawater throughout the sampled section. This observation is consistent with independent findings pointing to primary sediment detrital inputs of continental provenance<sup>18,20-23</sup>, reinforced by our stronger physical rather than chemical weathering indicators. This relationship is further strengthened by the association of average UCC profiles (Fig. S11) with the continental margin location of the sedimentary basin.

High Cr/Ti ratios recorded during the GOE were previously ascribed to mobilization of dissolved Cr from land to the ocean by acid rock drainage via the activity of acidophilic aerobic bacteria following oxygenation of the atmosphere<sup>27</sup>. A similar but previously unreported acidification event could explain the brief spike in Cr/Ti ratios in the

<figure><img src="image_15.png" /><figcaption>**Fig. 6** | Distribution of sample P concentration relative to fine grain marine siliciclastic sedimentary rock content through time².</figcaption></figure>

upper BDF. However, a close look at the data indicates that total P₂O₅ and Fe₂O₃ contents immediately before, during and after the transient increase in Cr/Ti ratios remained low, suggesting that even if this event was triggered by acidic weathering of terrestrial rocks, it cannot explain the behaviour, source, and mechanism of P₂O₅ enrichment in our samples.

Further, the highly soluble properties of ferrous and ferric Fe under extreme acidic conditions characteristic of acid rock drainage<sup>32</sup> should translate to relative co-enrichment of Fe and Cr in the sediments with respect to poorly mobile Ti. This relationship is not seen in the studied section. Moreover, the broad expression of similar but conservative Fe/Ti and P/Ti profiles throughout the BDF and the tillite formation are consistent with reported low to moderate chemical weathering indices in the tillites<sup>33</sup>. Thus, the combined data better reflect terrestrial detritus contributing to high bulk P₂O₅ and Fe₂O₃ enrichment in the PATF and the lower BDF section, assuming continental erosion by melting ice sheets was the principal source of detrital inputs into the sediment pile. Moreover, our bulk P data are consistent with historical records showing a substantial spike in the P content of Cryogenian fine-grained marine siliciclastic rocks² (Fig. 6).

## Highly reactive Fe and dissolved P chemistry

In light of the above discussions, we pose the question of whether P was associated with Fe in the primary sediments and, if so, whether such a relationship can provide insights into seawater-dissolved P profiles. The distribution of leachable highly reactive Fe (Fe<sub>HR</sub>) phases in the form of Fe-ox<sub>HR</sub> + pyrite Fe and poorly reactive sheet silicate Fe (Fig. 7a) in representative samples was therefore explored according to references<sup>34-36</sup> (see methods). Intriguingly, the Fe-ox<sub>HR</sub> phases decline by a factor of two when emerging from the Snowball ice sheet melting stage and transitioning into post-Snowball greenhouse state (Fig. 7b). The ratio of Fe-ox<sub>HR</sub> over total Fe content, suggest that Fe-ox<sub>HR</sub> constitutes only a small proportion of total Fe across the sequence, with distinct fluctuations that parallel low pre-Snowball P₂O₅, immediate post-Snowball high P₂O₅ and late post-Snowball low P₂O₅ intervals (Fig. 7c). A similar pattern is noted when Fe-ox<sub>HR</sub> concentrations are compared to unreactive sheet silicate Fe content, with the data suggesting that the majority of Fe throughout the sampled stratigraphy is largely present as unreactive silicates. These data are consistent with the above observations pointing to significant detrital contribution to sediment Fe enrichment, as opposed to chemical sedimentation.

Bulk sediment P analysis, as shown by our results, provides important clues on the overall behaviour of P in marine waters<sup>1,2,37,38</sup>. However, bulk sediment P content is a poor differentiator of reactive and unreactive P composition and therefore is an unreliable indicator of P bioavailability. Instead, we consider the linear correlation between
correlations between TiO₂, P₂O₅ and Fe₂O₃ for tillites and post-Snowball facies may consequently be the result of sediment source homogenization by the indiscriminate erosional action of melting ice sheets. Regardless, these observations provide further evidence for across sequence P₂O₅ and Fe₂O₃ enrichment by detritus.

The low C<sub>org</sub> and negative δ<sup>13</sup>C<sub>carbonate</sub> distribution in the facies (Fig. 2 & S1-S2) suggest microbial oxidation of C<sub>org</sub> likely prevailed at the sediment-water interface, which would have promoted the release of organic-bound P into sea and sediment pore water, influencing dissolved aqueous P content and eventual incorporation into various sedimentary minerals. This would have been particularly relevant in the immediate post-Snowball interval where apatite formation became more pronounced, compared to the rest of the section (Fig. 3 & Table S2). It is also possible that prevailing environmental conditions influenced ongoing microbial transformation of P-rich C<sub>org</sub> and Fe-oxHR minerals to trigger enough diagenetic sediment porewater P supersaturation<sup>30</sup>. For example, the geochemical data suggest that bulk primary sediment P was predominantly associated with non-calcium bearing minerals such as Fe-oxHR and unreactive detrital silicate phases (Figs. S6-S9), which would have starved primary sediments of dissolved P. Except for some immediate post-Snowball samples, across-sequence CaO and P₂O₅ inverse correlations, being up to 79% for the tillites (Fig. S6a-b), corroborate limited potential P preservation in non-calcium bearing mineral phases. As discussed above, this view is supported by low LOI, low-carbonate facies associated with bulk high P₂O₅/Fe₂O₃ ratios and high LOI, high-carbonate lithologies with bulk low-P₂O₅/Fe₂O₃ ratios (Fig. S5). Overall decreasing P₂O₅ concentration coincides with C<sub>org</sub> content that increases from post-Snowball to pre-Snowball facies (Fig. S6c), signalling either possible diagenetic P enrichment or loss in primary sediments through microbial oxidation of organic-rich P biomass originating from the water column. Indeed, our lowest δ<sup>13</sup>C<sub>org</sub> and C<sub>org</sub> values in the tillites and immediate post-Snowball interval (Fig. 2a-b) coincide with P₂O₅ enrichment compared to the low P₂O₅ pre-Snowball samples (Fig. S6c-d). Based on these observations, microbial recycling of organic-rich P at the sediment-water interface could explain the increasing prevalence of apatite in the immediate post-Snowball interval. However, the data suggest that the P supersaturation required to spontaneously precipitate large amounts of apatite precursor phases and significant substitution in carbonate minerals<sup>30,31</sup> was limited, especially in the pre-Snowball interval. Instead, our results indicate that dominant P supply and enrichment in the primary sediments mostly reflect detrital loading with non-apatite minerals. Moreover, as we show below, the synthesis of Ca-rich P minerals was perhaps limited by abundant Fe-oxHR particles acting as efficient scavengers of dissolved PO₄³⁻ at the sediment seawater interface.

Redox-sensitive Mn shows a weak negative correlation with TiO₂ and Al₂O₃ across all facies (Fig. S10), suggesting that Mn enrichment pathways are to some extent decoupled from those of P₂O₅ and Fe₂O₃, particularly given the considerable positive correlation between P₂O₅, TiO₂, and Al₂O₃ (Fig. 5). Except for the short-lived spike in Cr enrichment in the upper BDF relative to Ti, overall, our data do not indicate that significant oxidative/chemical weathering of terrestrial rocks was a predominant mechanism for PO₄³⁻ delivery to seawater throughout the sampled section. This observation is consistent with independent findings pointing to primary sediment detrital inputs of continental provenance<sup>18,20-23</sup>, reinforced by our stronger physical rather than chemical weathering indicators. This relationship is further strengthened by the association of average UCC profiles (Fig. S11) with the continental margin location of the sedimentary basin.

High Cr/Ti ratios recorded during the GOE were previously ascribed to mobilization of dissolved Cr from land to the ocean by acid rock drainage via the activity of acidophilic aerobic bacteria following oxygenation of the atmosphere<sup>27</sup>. A similar but previously unreported acidification event could explain the brief spike in Cr/Ti ratios in the

<figure><img src="image_15.png" /><figcaption>**Fig. 6** | Distribution of sample P concentration relative to fine grain marine siliciclastic sedimentary rock content through time².</figcaption></figure>

upper BDF. However, a close look at the data indicates that total P₂O₅ and Fe₂O₃ contents immediately before, during and after the transient increase in Cr/Ti ratios remained low, suggesting that even if this event was triggered by acidic weathering of terrestrial rocks, it cannot explain the behaviour, source, and mechanism of P₂O₅ enrichment in our samples.

Further, the highly soluble properties of ferrous and ferric Fe under extreme acidic conditions characteristic of acid rock drainage<sup>32</sup> should translate to relative co-enrichment of Fe and Cr in the sediments with respect to poorly mobile Ti. This relationship is not seen in the studied section. Moreover, the broad expression of similar but conservative Fe/Ti and P/Ti profiles throughout the BDF and the tillite formation are consistent with reported low to moderate chemical weathering indices in the tillites<sup>33</sup>. Thus, the combined data better reflect terrestrial detritus contributing to high bulk P₂O₅ and Fe₂O₃ enrichment in the PATF and the lower BDF section, assuming continental erosion by melting ice sheets was the principal source of detrital inputs into the sediment pile. Moreover, our bulk P data are consistent with historical records showing a substantial spike in the P content of Cryogenian fine-grained marine siliciclastic rocks² (Fig. 6).

## Highly reactive Fe and dissolved P chemistry

In light of the above discussions, we pose the question of whether P was associated with Fe in the primary sediments and, if so, whether such a relationship can provide insights into seawater-dissolved P profiles. The distribution of leachable highly reactive Fe (FeHR) phases in the form of Fe-oxHR + pyrite Fe and poorly reactive sheet silicate Fe (Fig. 7a) in representative samples was therefore explored according to references<sup>34-36</sup> (see methods). Intriguingly, the Fe-oxHR phases decline by a factor of two when emerging from the Snowball ice sheet melting stage and transitioning into post-Snowball greenhouse state (Fig. 7b). The ratio of Fe-oxHR over total Fe content, suggest that Fe-oxHR constitutes only a small proportion of total Fe across the sequence, with distinct fluctuations that parallel low pre-Snowball P₂O₅, immediate post-Snowball high P₂O₅ and late post-Snowball low P₂O₅ intervals (Fig. 7c). A similar pattern is noted when Fe-oxHR concentrations are compared to unreactive sheet silicate Fe content, with the data suggesting that the majority of Fe throughout the sampled stratigraphy is largely present as unreactive silicates. These data are consistent with the above observations pointing to significant detrital contribution to sediment Fe enrichment, as opposed to chemical sedimentation.

Bulk sediment P analysis, as shown by our results, provides important clues on the overall behaviour of P in marine waters<sup>1,2,37,38</sup>. However, bulk sediment P content is a poor differentiator of reactive and unreactive P composition and therefore is an unreliable indicator of P bioavailability. Instead, we consider the linear correlation between
<figure><img src="image_16.png" /><figcaption>**Fig. 7 |** The distribution of reactive, poorly reactive, and unreactive Fe mineral phases. **a** Contribution of defined Fe mineral phases expressed as a percentage of total Fe content across sequence stratigraphy. **b** Contribution of highly reactive Fe oxyhydr(oxide) (Fe-oxHR), poorly reactive sheet silicate Fe, unreactive sheet silicate Fe and pyrite Fe, expressed as a fraction of total Fe content across sequence stratigraphy. **c** Fe-oxHR to total Fe ratio (Fe~T~) (Fe-oxHR/Fe~T~) and Fe-oxHR/unreactive Fe ratio. **d** Representative putative magnetite- and sheet silicate-bound P distribution</figcaption></figure>

across sequence stratigraphy. **e** Representative putative magnetite-bound P/Fe ratios across sequence stratigraphy. LLF, Lossit Limestone Formation. PATF, Port Askaig Tillite Formation. PAT, Port Askaig Tillites, where PAT1 and PAT2 represent tillites from the Port Askaig type location on Islay and PAT3 the LL-16-a sample at the top of the LLF that conformably underlines the Port Askaig tillites. BDF, Bonahaven Dolomite Formation.

Fe-oxHR-bound P and dissolved P (refs. 1,37–39), in modern marine systems as the best estimator of dissolved P behaviour during sediment deposition, following the recommendation of Thompson and others⁴⁰ (see methods). We found 0% of measurable leached P associated with the Fe carbonates, compared to ~9.1% for the combined goethite, akageneite and hematite phases (all post-Snowball); ~45.5% for magnetite (42.5% post-Snowball and 3.0% pre-Snowball); ~6.1% for hematite (all pre-Snowball); and 39.4% for the tillites and post-Snowball sheet silicates (Figs. S7 & S8).

The sheet silicates in the tillites and immediate post-Snowball, record the highest leachable P content. Overall, the distribution of P between the sheet silicates and the Fe-oxHR reservoir indicate that high P enrichment in association with sheet silicates at the terminal Snowball immediate post-Snowball greenhouse transition, is marked by redistribution of P to a putative magnetite sink (Fig. 7d). A corresponding ~twofold reduction in the size of the leachable Fe-oxHR inventory at this time would have reduced the potential removal efficiency of dissolved PO₄³⁻ from seawater by an equally similar magnitude, since Fe-oxHR is otherwise a strong P sink³⁷⁻³⁹. This process alone would have enabled substantial build-up of dissolved PO₄³⁻ in immediate post-Snowball seawater relative to the period before and after, both distinguished by a higher Fe-oxHR reservoir (Fig. 7b). Furthermore, the peaking of putative sheet silicate P in the tillites, which is hundreds of times above baseline detection concentrations of 5.47 ppb in the pre-Snowball interval, is consistent with rock flour production expected with the mechanical grinding action of melting ice sheets on the bedrock. This supposition is supported by SEM-EDS imaging showing elevated fine-grained sheet silicate clasts in the immediate post-Snowball samples (Fig. 3d).

We assume that the coincidental rise of appreciable P enrichment in immediate post-Snowball magnetite grains relative to the tillites interval, points to increasing immediate post-Snowball

co-precipitation of magnetite and dissolved PO₄³⁻ out of seawater. A test of this hypothesis finds that peaks in magnetite-associated P/Fe ratios correlate with the appearance and persistence of magnetite-bound P at the tillite post-Snowball boundary and upwards (Fig. 7d-e). This up-section correlation between magnetite-bound P concentration and magnetite P/Fe ratios, suggests magnetite precipitation captures a snapshot of the potential dissolved PO₄³⁻ content of the reservoir from which it formed. The distinctly variable but higher P/Fe values in the late low-P₂O₅ post-Snowball interval are best explained by emergent long-term moderate presence and persistence of magnetite-bound P in the facies (Fig. 7d). The mostly non-variant magnetite-bound P trend at this time, with the exception of a single spike, points to steady scavenging of PO₄³⁻ by an increasingly scarce magnetite reservoir, instead of a rise in dissolved PO₄³⁻ content.

The release of bound PO₄³⁻ to seawater and/or sediment pore water by diagenetic dissolution of Fe-oxHR minerals could, however, account for the two times smaller Fe-oxHR budget in the immediate post-Snowball P₂O₅-rich rocks, compared to the P₂O₅-depleted sediments that bracket this interval. Yet, because diagenesis results in considerable loss of Fe-oxHR-bound P, this interval should be accompanied by parallel lowering of sedimentary P₂O₅ and Fe-oxHR-associated P content if this were the case. Instead, we observe co-increase in both bulk P₂O₅ and potential magnetite-bound P at this time. Further, the comparatively lower pre/late post-Snowball P₂O₅ and magnetite P reservoirs cannot be explained by reductive dissolution of Fe-oxHR since their Fe-oxHR inventories are about twice the size found in the P₂O₅-rich immediate post-Snowball section. In addition, the transition of bulk Fe/Al ratios from the higher values expected with enhanced authigenic Fe enrichment during the pre-Snowball time to lower detrital Fe/Al ratios averaging ~0.5 in the tillites and for most of the post-Snowball sediments, is consistent with negligible reductive Fe mobilisation by diagenetic microbial Fe-reduction³⁴,⁴¹,⁴². Importantly,
<figure><img src="image_16.png" /><figcaption>**Fig. 7 |** The distribution of reactive, poorly reactive, and unreactive Fe mineral phases. **a** Contribution of defined Fe mineral phases expressed as a percentage of total Fe content across sequence stratigraphy. **b** Contribution of highly reactive Fe oxyhydr(oxide) (Fe-oxHR), poorly reactive sheet silicate Fe, unreactive sheet silicate Fe and pyrite Fe, expressed as a fraction of total Fe content across sequence stratigraphy. **c** Fe-oxHR to total Fe ratio (Fe~T~) (Fe-oxHR/Fe~T~) and Fe-oxHR/unreactive Fe ratio. **d** Representative putative magnetite- and sheet silicate-bound P distribution</figcaption></figure>

across sequence stratigraphy. **e** Representative putative magnetite-bound P/Fe ratios across sequence stratigraphy. LLF, Lossit Limestone Formation. PATF, Port Askaig Tillite Formation. PAT, Port Askaig Tillites, where PAT1 and PAT2 represent tillites from the Port Askaig type location on Islay and PAT3 the LL-16-a sample at the top of the LLF that conformably underlines the Port Askaig tillites. BDF, Bonahaven Dolomite Formation.

Fe-oxHR-bound P and dissolved P (refs. 1,37–39), in modern marine systems as the best estimator of dissolved P behaviour during sediment deposition, following the recommendation of Thompson and others⁴⁰ (see methods). We found 0% of measurable leached P associated with the Fe carbonates, compared to ~9.1% for the combined goethite, akageneite and hematite phases (all post-Snowball); ~45.5% for magnetite (42.5% post-Snowball and 3.0% pre-Snowball); ~6.1% for hematite (all pre-Snowball); and 39.4% for the tillites and post-Snowball sheet silicates (Figs. S7 & S8).

The sheet silicates in the tillites and immediate post-Snowball, record the highest leachable P content. Overall, the distribution of P between the sheet silicates and the Fe-oxHR reservoir indicate that high P enrichment in association with sheet silicates at the terminal Snowball immediate post-Snowball greenhouse transition, is marked by redistribution of P to a putative magnetite sink (Fig. 7d). A corresponding ~twofold reduction in the size of the leachable Fe-oxHR inventory at this time would have reduced the potential removal efficiency of dissolved PO₄³⁻ from seawater by an equally similar magnitude, since Fe-oxHR is otherwise a strong P sink³⁷⁻³⁹. This process alone would have enabled substantial build-up of dissolved PO₄³⁻ in immediate post-Snowball seawater relative to the period before and after, both distinguished by a higher Fe-oxHR reservoir (Fig. 7b). Furthermore, the peaking of putative sheet silicate P in the tillites, which is hundreds of times above baseline detection concentrations of 5.47 ppb in the pre-Snowball interval, is consistent with rock flour production expected with the mechanical grinding action of melting ice sheets on the bedrock. This supposition is supported by SEM-EDS imaging showing elevated fine-grained sheet silicate clasts in the immediate post-Snowball samples (Fig. 3d).

We assume that the coincidental rise of appreciable P enrichment in immediate post-Snowball magnetite grains relative to the tillites interval, points to increasing immediate post-Snowball

co-precipitation of magnetite and dissolved PO₄³⁻ out of seawater. A test of this hypothesis finds that peaks in magnetite-associated P/Fe ratios correlate with the appearance and persistence of magnetite-bound P at the tillite post-Snowball boundary and upwards (Fig. 7d-e). This up-section correlation between magnetite-bound P concentration and magnetite P/Fe ratios, suggests magnetite precipitation captures a snapshot of the potential dissolved PO₄³⁻ content of the reservoir from which it formed. The distinctly variable but higher P/Fe values in the late low-P₂O₅ post-Snowball interval are best explained by emergent long-term moderate presence and persistence of magnetite-bound P in the facies (Fig. 7d). The mostly non-variant magnetite-bound P trend at this time, with the exception of a single spike, points to steady scavenging of PO₄³⁻ by an increasingly scarce magnetite reservoir, instead of a rise in dissolved PO₄³⁻ content.

The release of bound PO₄³⁻ to seawater and/or sediment pore water by diagenetic dissolution of Fe-oxHR minerals could, however, account for the two times smaller Fe-oxHR budget in the immediate post-Snowball P₂O₅-rich rocks, compared to the P₂O₅-depleted sediments that bracket this interval. Yet, because diagenesis results in considerable loss of Fe-oxHR-bound P, this interval should be accompanied by parallel lowering of sedimentary P₂O₅ and Fe-oxHR-associated P content if this were the case. Instead, we observe co-increase in both bulk P₂O₅ and potential magnetite-bound P at this time. Further, the comparatively lower pre/late post-Snowball P₂O₅ and magnetite P reservoirs cannot be explained by reductive dissolution of Fe-oxHR since their Fe-oxHR inventories are about twice the size found in the P₂O₅-rich immediate post-Snowball section. In addition, the transition of bulk Fe/Al ratios from the higher values expected with enhanced authigenic Fe enrichment during the pre-Snowball time to lower detrital Fe/Al ratios averaging ~0.5 in the tillites and for most of the post-Snowball sediments, is consistent with negligible reductive Fe mobilisation by diagenetic microbial Fe-reduction³⁴,⁴¹,⁴². Importantly,
the enrichment of P in the leachable immediate post-Snowball magnetite reservoir, which comes after a rise in associated sheet silicate-bound P, is best explained by transfer of sheet silicate-bound P to seawater, followed by chemical enrichment in the sediment pile by Fe-oxHR produced in the greenhouse interval.

Our estimates are conservative within reasonable error margins, considering that the designation of extractable Fe-oxHR phases in the defined Fe mineral pools can at times be misleading. For example, goethite was previously detected in the ammonium oxalate extract attributed to magnetite<sup>43</sup>. Our data are nonetheless consistent with SEM-EDS mineral imaging and bulk XRD mineralogical analysis, which failed to detect putative goethite-enriched phases as a major mineral constituent in the samples, suggesting an absence or low levels below detection. Instead, putative crystalline magnetite grains were observed in the immediate post-Snowball section, but rarely in the tillites and the pre- and post-Snowball intervals, interpreted as either an absence or very low concentrations (Fig. S9). This observation is consistent with potential pre-Snowball magnetite contributing only an estimated ~5.4% P to the total extractable P pool, compared to up to 37.8% for the post-Snowball time.

## Magnetite precipitation and seawater dissolved P behaviour

Magnetite, a common Fe mineral in Precambrian Fe-rich sedimentary rocks, often forms through a combination of biotic and abiotic processes involving ferrihydrite and green rust precursors<sup>44-48</sup>. In this light, green rust and ferrihydrite are thought to sequester and bury dissolved seawater trace nutrients in the sedimentary pile<sup>49,50</sup>. Particularly, the ability for both green rust and ferrihydrite to bind aqueous PO₄³⁻ has been demonstrated experimentally<sup>37-39,51-54</sup>, with green rust reported to possess a greater propensity to bind PO₄³⁻ than ferric Fe<sup>35</sup>. It is thus reasonable to assume that the incorporation of P into magnetite crystals scaled proportionally with the concentration of primary seawater green rust and ferrihydrite magnetite precursors.

Nonetheless, although prograde metamorphism exerts a negligible effect on magnetite transformation, it can become significant in the presence of olivine<sup>55,56</sup>. Mineralogical appraisal of our samples by XRD and SEM-EDS mapping, however failed to identify olivine as an important mineral phase throughout the sequence, while the influence of hydrothermal fluids on Fe distribution appears to be insignificant (see Fig. S3). Moreover, a lack of covariation between carbonate Fe and magnetite Fe reservoirs across sequence stratigraphy, further suggests little or no thermal breakdown of Fe carbonates to magnetite by burial metamorphism<sup>57</sup>. Importantly, spontaneous binding of PO₄³⁻ to magnetite occurs by physical adsorptive intermolecular attractive forces and by chemical transfer of electrons between magnetite and PO₄³⁻ molecules, promoting an adsorption capacity of ~57.8 mg of PO₄³⁻ per gram and resulting in a positive correlation between magnetite-bound and dissolved PO₄³⁻ (ref. 13). This binding of dissolved PO₄³⁻ by magnetite enhances magnetite's stability<sup>12,13</sup> and therefore enhancement of possible long-term preservation in sediments.

We can only speculate that the prevalence of putative magnetite grains, particularly in the immediate post-glacial P₂O₅-rich interval, compared to the low P₂O₅ intervals, reflects nascent post-glacial seawater conditions, probably related to the balance between seawater oxygen content and local Fe sedimentary mechanisms. For instance, modern turbid Arctic glacial outflows generally display high dissolved Fe content of up to 20 µM, which decreases to nanomolar concentrations at the shelf-fjord water mixing boundary<sup>58</sup>. This trend results from rapid flocculation of dissolved Fe at this interface and the binding of particle surfaces because of increasing salinity and pH, triggering the loss of up to 98% total dissolved Fe (refs. 58,59). Similar rapid precipitation of particulate Fe with increasing oxygenation at Snowball melt water-seawater interfaces would have accelerated the scavenging of dissolved P released by clay minerals along the gradients of rising salinity and pH in the continental margin waters<sup>5,6</sup>.

Although we are unable to quantitatively distinguish the extent of Fe(II) oxidation at the end-Snowball post-Snowball transition, predominantly positive δ⁵⁶Febulk sedimentary values (Table S4) indicate that partial Fe(II) oxidation<sup>60</sup> was common throughout the deposition of the studied sequence. This process would have favoured preferential formation of magnetite as allowed by local thermodynamic conditions of redox, electrical conductivity, pH, and temperature<sup>61,62</sup>. For instance, magnetite precipitation and stability may have been favoured at the lower temperatures and pH conditions that accompanied the immediate post-glacial CO₂-rich world<sup>61,62</sup>. It is also possible that the reduction of ferrihydrite by biomass to magnetite could have been common<sup>45,47</sup>. However, the absence of strong negative δ⁵⁶Fe signatures across the studied profile is consistent with overall negligible diagenetic production of magnetite and Fe carbonates via dissimilatory microbial reduction of Fe-oxHR. Thus, considering the linear relationship existing between magnetite-bound and aqueous PO₄³⁻ (ref. 12), PO₄³⁻ bioavailability in the immediate post-Snowball waters potentially increased by at least 20-fold compared to pre-Snowball conditions. Unlike the immediate post-Snowball interval, putative immediate pre-Snowball magnetite-bound P remained below the instrument detection limit of ~5 ppb, with the data indicating that unreactive silicate-bound P dominated bulk P burial before and during the Sturtian Snowball (Fig. S7).

## Implications for seawater redox

Carbonate-rich samples with <5% Fe content tend to produce anomalously high FeHR/FeT ratios<sup>34</sup>. The reconstructed Fe-based redox trends were therefore evaluated for deviations as a function of Fe and carbonate content. The absence of significant differences regardless of total Fe and carbonate content resulting in consistent trends along sequence stratigraphy, was taken to imply a negligible impact of carbonate content on the reliability of the Fe-based redox proxy. We further interpret the general lack of significant deviations in the Fe-based redox proxy profiles as a reflection of the significant siliciclastic and Fe-rich content of the studied lithologies<sup>18-23</sup>, including those containing carbonates, as established by our geochemical analyses. The impact of sedimentation rates was determined to be negligible, considering that estimated values are four times lower than those expected to compromise the sensitivity of the Fe-based redox proxy<sup>34</sup> (see supplementary information).

Average FeHR/FeT ratios are 0.55 ± 0.21, 0.16 ± 0.04, and 0.68 ± 0.30 for the pre-Snowball and tillites, the P₂O₅-rich immediate post-Snowball, and the P₂O₅-poor late post-Snowball intervals, respectively (Fig. 8a). Their corresponding average FePy/FeT ratios are 0.21 ± 0.22, 0.31 ± 0.34, and 0.42 ± 0.31, respectively (Fig. 8b). The FePy/FeHR ratios of <0.8 suggest deposition of the entire sediment profile in mainly ferruginous-like conditions, although the FeHR/FeT ratios of <0.22 in the immediate post-Snowball interval are consistent with oxygenated waters, while the >0.38 FeHR/FeT ratios indicate anoxic bottom water depositional conditions for the pre-Snowball, tillite, and late post-Snowball samples<sup>34-36</sup>. Average FeHR/FeT values for samples straddling the peak post-glacial P₂O₅ interlude correlate negatively with their associated magnetite-bound P values, implying rising magnetite-bound P values coincide with lower FeHR/FeT ratios associated with oxic waters (Fig. 8c). No such correlation is observed for the pre-Snowball, tillites and late post-Snowball samples. These observations provide substantial evidence that the transitory rise in sedimentary P₂O₅ content in the immediate post-Snowball sediments was likely attended by transient seawater oxygenation and that magnetite indeed records dissolved seawater PO₄³⁻ dynamics at this time.

The oxygenation trends are further highlighted by temporal Fe/Al profiles across the sequence<sup>34,41,42,63</sup> (Fig. 8d). In this regard, the >0.5 pre-Snowball Fe/Al ratios are generally consistent with higher sediment pyrite enrichments, compared to tillites samples and the immediate post-Snowball facies, which are depleted in pyrite
the enrichment of P in the leachable immediate post-Snowball magnetite reservoir, which comes after a rise in associated sheet silicate-bound P, is best explained by transfer of sheet silicate-bound P to seawater, followed by chemical enrichment in the sediment pile by Fe-oxHR produced in the greenhouse interval.

Our estimates are conservative within reasonable error margins, considering that the designation of extractable Fe-oxHR phases in the defined Fe mineral pools can at times be misleading. For example, goethite was previously detected in the ammonium oxalate extract attributed to magnetite<sup>43</sup>. Our data are nonetheless consistent with SEM-EDS mineral imaging and bulk XRD mineralogical analysis, which failed to detect putative goethite-enriched phases as a major mineral constituent in the samples, suggesting an absence or low levels below detection. Instead, putative crystalline magnetite grains were observed in the immediate post-Snowball section, but rarely in the tillites and the pre- and post-Snowball intervals, interpreted as either an absence or very low concentrations (Fig. S9). This observation is consistent with potential pre-Snowball magnetite contributing only an estimated -5.4% P to the total extractable P pool, compared to up to 37.8% for the post-Snowball time.

## Magnetite precipitation and seawater dissolved P behaviour

Magnetite, a common Fe mineral in Precambrian Fe-rich sedimentary rocks, often forms through a combination of biotic and abiotic processes involving ferrihydrite and green rust precursors<sup>44-48</sup>. In this light, green rust and ferrihydrite are thought to sequester and bury dissolved seawater trace nutrients in the sedimentary pile<sup>49,50</sup>. Particularly, the ability for both green rust and ferrihydrite to bind aqueous PO₄³⁻ has been demonstrated experimentally<sup>37-39,51-54</sup>, with green rust reported to possess a greater propensity to bind PO₄³⁻ than ferric Fe<sup>35</sup>. It is thus reasonable to assume that the incorporation of P into magnetite crystals scaled proportionally with the concentration of primary seawater green rust and ferrihydrite magnetite precursors.

Nonetheless, although prograde metamorphism exerts a negligible effect on magnetite transformation, it can become significant in the presence of olivine<sup>55,56</sup>. Mineralogical appraisal of our samples by XRD and SEM-EDS mapping, however failed to identify olivine as an important mineral phase throughout the sequence, while the influence of hydrothermal fluids on Fe distribution appears to be insignificant (see Fig. S3). Moreover, a lack of covariation between carbonate Fe and magnetite Fe reservoirs across sequence stratigraphy, further suggests little or no thermal breakdown of Fe carbonates to magnetite by burial metamorphism<sup>57</sup>. Importantly, spontaneous binding of PO₄³⁻ to magnetite occurs by physical adsorptive intermolecular attractive forces and by chemical transfer of electrons between magnetite and PO₄³⁻ molecules, promoting an adsorption capacity of ~57.8 mg of PO₄³⁻ per gram and resulting in a positive correlation between magnetite-bound and dissolved PO₄³⁻ (ref. 13). This binding of dissolved PO₄³⁻ by magnetite enhances magnetite's stability<sup>12,13</sup> and therefore enhancement of possible long-term preservation in sediments.

We can only speculate that the prevalence of putative magnetite grains, particularly in the immediate post-glacial P₂O₅-rich interval, compared to the low P₂O₅ intervals, reflects nascent post-glacial seawater conditions, probably related to the balance between seawater oxygen content and local Fe sedimentary mechanisms. For instance, modern turbid Arctic glacial outflows generally display high dissolved Fe content of up to 20 µM, which decreases to nanomolar concentrations at the shelf-fjord water mixing boundary<sup>58</sup>. This trend results from rapid flocculation of dissolved Fe at this interface and the binding of particle surfaces because of increasing salinity and pH, triggering the loss of up to 98% total dissolved Fe (refs. 58,59). Similar rapid precipitation of particulate Fe with increasing oxygenation at Snowball melt water-seawater interfaces would have accelerated the scavenging of dissolved P released by clay minerals along the gradients of rising salinity and pH in the continental margin waters<sup>5,6</sup>.

Although we are unable to quantitatively distinguish the extent of Fe(II) oxidation at the end-Snowball post-Snowball transition, predominantly positive δ⁵⁶Febulk sedimentary values (Table S4) indicate that partial Fe(II) oxidation<sup>60</sup> was common throughout the deposition of the studied sequence. This process would have favoured preferential formation of magnetite as allowed by local thermodynamic conditions of redox, electrical conductivity, pH, and temperature<sup>61,62</sup>. For instance, magnetite precipitation and stability may have been favoured at the lower temperatures and pH conditions that accompanied the immediate post-glacial CO₂-rich world<sup>61,62</sup>. It is also possible that the reduction of ferrihydrite by biomass to magnetite could have been common<sup>45,47</sup>. However, the absence of strong negative δ⁵⁶Fe signatures across the studied profile is consistent with overall negligible diagenetic production of magnetite and Fe carbonates via dissimilatory microbial reduction of Fe-oxHR. Thus, considering the linear relationship existing between magnetite-bound and aqueous PO₄³⁻ (ref. 12), PO₄³⁻ bioavailability in the immediate post-Snowball waters potentially increased by at least 20-fold compared to pre-Snowball conditions. Unlike the immediate post-Snowball interval, putative immediate pre-Snowball magnetite-bound P remained below the instrument detection limit of ~5 ppb, with the data indicating that unreactive silicate-bound P dominated bulk P burial before and during the Sturtian Snowball (Fig. S7).

## Implications for seawater redox

Carbonate-rich samples with <5% Fe content tend to produce anomalously high FeHR/FeT ratios<sup>34</sup>. The reconstructed Fe-based redox trends were therefore evaluated for deviations as a function of Fe and carbonate content. The absence of significant differences regardless of total Fe and carbonate content resulting in consistent trends along sequence stratigraphy, was taken to imply a negligible impact of carbonate content on the reliability of the Fe-based redox proxy. We further interpret the general lack of significant deviations in the Fe-based redox proxy profiles as a reflection of the significant siliciclastic and Fe-rich content of the studied lithologies<sup>18-23</sup>, including those containing carbonates, as established by our geochemical analyses. The impact of sedimentation rates was determined to be negligible, considering that estimated values are four times lower than those expected to compromise the sensitivity of the Fe-based redox proxy<sup>34</sup> (see supplementary information).

Average FeHR/FeT ratios are 0.55 ± 0.21, 0.16 ± 0.04, and 0.68 ± 0.30 for the pre-Snowball and tillites, the P₂O₅-rich immediate post-Snowball, and the P₂O₅-poor late post-Snowball intervals, respectively (Fig. 8a). Their corresponding average FePy/FeT ratios are 0.21 ± 0.22, 0.31 ± 0.34, and 0.42 ± 0.31, respectively (Fig. 8b). The FePy/FeHR ratios of <0.8 suggest deposition of the entire sediment profile in mainly ferruginous-like conditions, although the FeHR/FeT ratios of <0.22 in the immediate post-Snowball interval are consistent with oxygenated waters, while the >0.38 FeHR/FeT ratios indicate anoxic bottom water depositional conditions for the pre-Snowball, tillite, and late post-Snowball samples<sup>34-36</sup>. Average FeHR/FeT values for samples straddling the peak post-glacial P₂O₅ interlude correlate negatively with their associated magnetite-bound P values, implying rising magnetite-bound P values coincide with lower FeHR/FeT ratios associated with oxic waters (Fig. 8c). No such correlation is observed for the pre-Snowball, tillites and late post-Snowball samples. These observations provide substantial evidence that the transitory rise in sedimentary P₂O₅ content in the immediate post-Snowball sediments was likely attended by transient seawater oxygenation and that magnetite indeed records dissolved seawater PO₄³⁻ dynamics at this time.

The oxygenation trends are further highlighted by temporal Fe/Al profiles across the sequence<sup>34,41,42,63</sup> (Fig. 8d). In this regard, the >0.5 pre-Snowball Fe/Al ratios are generally consistent with higher sediment pyrite enrichments, compared to tillites samples and the immediate post-Snowball facies, which are depleted in pyrite
<figure><img src="image_17.png" /><figcaption>**Fig. 8 | Redox reconstruction.** *a* Fe<sub>HR</sub>/Fe<sub>T</sub> ratios. *b* Fe<sub>PY</sub>/Fe<sub>T</sub> ratios. *c* Relationship between associated magnetite-bound P and Fe speciation. *d* Fe/Al trend for the studied section. *e* Numerical model with riverine P input increased by 40-60% relative to present day for 5 Myr. *f* Numerical model for atmosphere and deep ocean oxygen reservoirs for river input scenario. *g* Numerically modelled fraction of oxic seafloor in the proximal and distal shelf environments for river input scenario. *h* Numerical model when riverine P input is held constant relative to present day, while a further 40-60% of background P flux is added to ocean interior. *i* Numerical model for atmosphere and deep ocean oxygen reservoirs for ocean</figcaption></figure>

interior input scenario. *j* Numerically modelled fraction of oxic seafloor in the proximal and distal shelf environments for ocean interior input scenario. *k-l* Numerically modelled P burial fluxes in the deep ocean, proximal shelf, and distal shelf environments. *m-n* Numerically modelled total marine P concentration. Note that interior ocean P release results in a higher marine P inventory by avoiding rapid burial in the proximal zone. For full details of the model, see methods and references<sup>63,64</sup>. LLF, Lossit Limestone Formation. PATF, Port Askaig Tillite Formation. BDF, Bonahaven Dolomite Formation.

(Figs. 7b & 8b). Such high Fe/Al values have been linked to the deposition of anoxic sediments beneath modern sulphide-enriched seawater, and lower values characterize oxic settings with limited $C_{org}$ supply to sediments<sup>41,42</sup>. Due to persistent supply of continental detritus as shown above, together with overall sedimentation rates that do not compromise the Fe<sub>HR</sub>/Fe<sub>T</sub> proxy as discussed in the supplementary information, the >0.5 Fe/Al ratios are best explained by syngenetic changes in anoxic pyrite precipitation. The <0.5 Fe/Al ratios, however, do not effectively delineate the pyrite-poor anoxic tillites from the apparently oxic immediate post-Snowball deposit (Fig. 8a), possibly due to increase input of Al-rich detritus during deposition of the tillites and immediate post-Snowball facies (Fig. 4b). Similarly, <0.5 Fe/Al ratios in the anoxic pyrite-poor late post-Snowball interval, as also suggested by the Fe<sub>HR</sub>/Fe<sub>T</sub> redox proxy, are followed by a small >0.5 Fe/Al spike corresponding to anoxic conditions (Fig. 8a) and pyrite enrichment at the top of the section (Figs. 7b, 8b & 8d).

Furthermore, a numerical biogeochemical model<sup>64,65</sup> (see methods) replicates the observed temporal rise and fall in seawater $PO_4^{3-}$ content and the transient immediate-post Snowball oxygenation event (Fig. 8e-j). The model which considers abrupt large input of riverine $PO_4^{3-}$ to near continental margin waters and the deep ocean, suggests that the initial considerable introduction of $PO_4^{3-}$ to continental margin waters could have briefly triggered seawater deoxygenation due to eutrophication (Fig. 8i). We note that the early rise in sedimentary $P_2O_5$ content was not immediately accompanied by seawater oxygenation. Moreover, the model shows that rising dissolved seawater $PO_4^{3-}$ concentration would have promoted increased $PO_4^{3-}$ burial, with subsequent decline in supply resulting in seawater deoxygenation (Fig. 8k-n), similar to our observations.

Our data reveal bulk P content comparable to previously published concentrations for fine grain siliciclastic Cryogenian facies. These data suggest that Cryogenian continental seawater P

bioavailability before, during, and after the Sturtian glaciations may have been limited by persistent detrital and variable Fe-Ox<sub>HR</sub> loading. Further, microbial recycling of organic-rich P at the primary sediment-water interface was insufficient to generate sediment porewater P saturation to spontaneously trigger vast precipitation of calcium-bearing P minerals across the sequence. This observation limits potential diagenetic interference with primary sediment P content. Production of dissolved sheet silicate bound $PO_4^{3-}$ would have been facilitated by grinding of the bedrock by thawing ice sheets, with the generation of sub-glacial acidity<sup>66</sup>. These subglacial acidic conditions, combined with acidic water produced by the immediate post-Snowball high $CO_2$ atmosphere<sup>67</sup>, would have sustained chemical leaching of P from rocks, including apatite minerals<sup>68</sup>. The sheet silicate clay minerals that are expected to more easily bind $PO_4^{3-}$ in more acidic conditions<sup>4-6</sup> transported and liberated bound $PO_4^{3-}$ to seawater following contact with higher marine pH<sup>5,6,10</sup> and salinity<sup>11,17</sup>. The sudden decline in leachable sheet silicate P entering the immediate post-Snowball state, followed by abrupt rise in magnetite P content by at least a factor of 200 compared to Pre-Snowball hints at a potential switch in P sink from clays to seawater. The increase in dissolved seawater P promoted primary productivity and oxygenation, with the resultant recycled biomass P captured together with dissolved inorganic P and preserved by Fe-Ox<sub>HR</sub> minerals generated in the oxidized water column (Fig. 9). Taken together, the data indicate a major switch from marine waters with low dissolved $PO_4^{3-}$ content to an enlarged inventory created by a deglaciating Cryogenian Snowball clay factory.

## Methods

### Sampling and sample preparation

Outcrop sampled lithologies and their locations are described in Table S1. Only a subset of representative rocks were analyzed for this study, but the overall collection was used to establish the placement of
<figure><img src="image_17.png" /><figcaption>**Fig. 8 | Redox reconstruction.** *a* Fe<sub>HR</sub>/Fe<sub>T</sub> ratios. *b* Fe<sub>PY</sub>/Fe<sub>T</sub> ratios. *c* Relationship between associated magnetite-bound P and Fe speciation. *d* Fe/Al trend for the studied section. *e* Numerical model with riverine P input increased by 40-60% relative to present day for 5 Myr. *f* Numerical model for atmosphere and deep ocean oxygen reservoirs for river input scenario. *g* Numerically modelled fraction of oxic seafloor in the proximal and distal shelf environments for river input scenario. *h* Numerical model when riverine P input is held constant relative to present day, while a further 40-60% of background P flux is added to ocean interior. *i* Numerical model for atmosphere and deep ocean oxygen reservoirs for ocean</figcaption></figure>

interior input scenario. *j* Numerically modelled fraction of oxic seafloor in the proximal and distal shelf environments for ocean interior input scenario. *k-l* Numerically modelled P burial fluxes in the deep ocean, proximal shelf, and distal shelf environments. *m-n* Numerically modelled total marine P concentration. Note that interior ocean P release results in a higher marine P inventory by avoiding rapid burial in the proximal zone. For full details of the model, see methods and references<sup>63,64</sup>. LLF, Lossit Limestone Formation. PATF, Port Askaig Tillite Formation. BDF, Bonahaven Dolomite Formation.

(Figs. 7b & 8b). Such high Fe/Al values have been linked to the deposition of anoxic sediments beneath modern sulphide-enriched seawater, and lower values characterize oxic settings with limited $C_{org}$ supply to sediments<sup>41,42</sup>. Due to persistent supply of continental detritus as shown above, together with overall sedimentation rates that do not compromise the Fe<sub>HR</sub>/Fe<sub>T</sub> proxy as discussed in the supplementary information, the >0.5 Fe/Al ratios are best explained by syngenetic changes in anoxic pyrite precipitation. The <0.5 Fe/Al ratios, however, do not effectively delineate the pyrite-poor anoxic tillites from the apparently oxic immediate post-Snowball deposit (Fig. 8a), possibly due to increase input of Al-rich detritus during deposition of the tillites and immediate post-Snowball facies (Fig. 4b). Similarly, <0.5 Fe/Al ratios in the anoxic pyrite-poor late post-Snowball interval, as also suggested by the Fe<sub>HR</sub>/Fe<sub>T</sub> redox proxy, are followed by a small >0.5 Fe/Al spike corresponding to anoxic conditions (Fig. 8a) and pyrite enrichment at the top of the section (Figs. 7b, 8b & 8d).

Furthermore, a numerical biogeochemical model<sup>64,65</sup> (see methods) replicates the observed temporal rise and fall in seawater $PO_4^{3-}$ content and the transient immediate-post Snowball oxygenation event (Fig. 8e-j). The model which considers abrupt large input of riverine $PO_4^{3-}$ to near continental margin waters and the deep ocean, suggests that the initial considerable introduction of $PO_4^{3-}$ to continental margin waters could have briefly triggered seawater deoxygenation due to eutrophication (Fig. 8i). We note that the early rise in sedimentary $P_2O_5$ content was not immediately accompanied by seawater oxygenation. Moreover, the model shows that rising dissolved seawater $PO_4^{3-}$ concentration would have promoted increased $PO_4^{3-}$ burial, with subsequent decline in supply resulting in seawater deoxygenation (Fig. 8k-n), similar to our observations.

Our data reveal bulk P content comparable to previously published concentrations for fine grain siliciclastic Cryogenian facies. These data suggest that Cryogenian continental seawater P

bioavailability before, during, and after the Sturtian glaciations may have been limited by persistent detrital and variable Fe-Ox<sub>HR</sub> loading. Further, microbial recycling of organic-rich P at the primary sediment-water interface was insufficient to generate sediment porewater P saturation to spontaneously trigger vast precipitation of calcium-bearing P minerals across the sequence. This observation limits potential diagenetic interference with primary sediment P content. Production of dissolved sheet silicate bound $PO_4^{3-}$ would have been facilitated by grinding of the bedrock by thawing ice sheets, with the generation of sub-glacial acidity<sup>66</sup>. These subglacial acidic conditions, combined with acidic water produced by the immediate post-Snowball high $CO_2$ atmosphere<sup>67</sup>, would have sustained chemical leaching of P from rocks, including apatite minerals<sup>68</sup>. The sheet silicate clay minerals that are expected to more easily bind $PO_4^{3-}$ in more acidic conditions<sup>4-6</sup> transported and liberated bound $PO_4^{3-}$ to seawater following contact with higher marine pH<sup>5,6,10</sup> and salinity<sup>11,17</sup>. The sudden decline in leachable sheet silicate P entering the immediate post-Snowball state, followed by abrupt rise in magnetite P content by at least a factor of 200 compared to Pre-Snowball hints at a potential switch in P sink from clays to seawater. The increase in dissolved seawater P promoted primary productivity and oxygenation, with the resultant recycled biomass P captured together with dissolved inorganic P and preserved by Fe-Ox<sub>HR</sub> minerals generated in the oxidized water column (Fig. 9). Taken together, the data indicate a major switch from marine waters with low dissolved $PO_4^{3-}$ content to an enlarged inventory created by a deglaciating Cryogenian Snowball clay factory.

## Methods

### Sampling and sample preparation

Outcrop sampled lithologies and their locations are described in Table S1. Only a subset of representative rocks were analyzed for this study, but the overall collection was used to establish the placement of
<figure><img src="image_18.png" /><figcaption>**Fig. 9 | A conceptual model for P cycling across the Sturtian Snowball glaciation.** The model highlights the relationship between glacially generated clays, P and Fe.</figcaption></figure>

samples along sequence stratigraphy. Prior to geochemical analysis, the outer exposed layers of samples were removed and only the unweathered portions were used for analysis. A fraction was milled into a fine powder for geochemical, chemostratigraphic and XRD mineralogical analyses. Slices of whole rock samples were thin sectioned and polished for scanning electron microscopy-energy dispersive spectroscopy (SEM-EDS).

## Mineralogical analysis

X-ray diffraction (XRD) analysis for bulk semi-quantitative qualitative mineralogy analysis was undertaken with a PANalytical Xpert-pro and a Bruker D8 ADVANCE diffractometers at Cardiff University and University of Poitiers, respectively, as previously described⁶⁹⁻⁷¹. SEM-EDS analysis was performed with an Oxford FEI-XL30 fitted Environmental SEM (ESEM) connected to an EDS system at Cardiff University. Analyses were conducted on polished thin sections coated with carbon to a thickness of 14 nm with a BIO-RAD SC500 sputter. The SEM-EDS analyses were run at a working distance of 8.9 mm and a 15 kV accelerating voltage. Backscattered elemental maps, point-specific atomic composition and spectra were combined to identify putative mineral phases. Semi-quantitative XRD analyses of the relative abundance of the mineral assemblages was calculated using the integrated area ratios of the principal peaks after decomposition by the FYTIK program⁷².

## Elemental analysis

An approximate 250 mg of bulk rock powders were dissolved using reagent grade acids in closed screw-top Teflon vessels (Savillex) at 90 °C for one day in concentrated 3 ml 40% HF, 3 ml 32% HCl, and 1 ml 65% HNO₃. Excess HF was neutralised with 93 ml H₃BO₃ (20 g/L) aqueous solution. Elements were measured by inductively coupled plasma atomic emission spectrometry (ICP-AES) using a Horiba Jobin Yvon® Ultima 2 spectrometer with boron as an internal standard. Calibrations were made with ACE, JB2, and WSE international standards, with relative standard deviation of ≤1% for SiO₂, ≤2% for the other major elements, and ≤5% for traces elements.

## Iron speciation analysis

Chemical extraction of sediment Fe phases was conducted using the sequential Fe extraction protocol of Poulton and Canfield and Fe measured using the ferrozine method³⁴⁻³⁶. Redox trends were further constrained using the distribution of Fe/Al ratios across the studied

section, where average ratios of ~0.55 ± 0.11 are common for oxic waters, with much greater values for anoxic settings³⁴⁻³⁶. Sediment Al/ (Al+Fe+Mn) content was used to demonstrate that hydrothermal contribution²⁵ of Fe to the sediments was negligible and that observed high Fe/Al ratios cannot be associated with hydrothermal activity. The sequential Fe extraction procedure resulted in the quantification of eight operationally defined Fe phases: (1) Total bulk rock Fe (FeT) from whole rock dissolved powder using hydrofluoric acid (HF); (2) Poorly reactive sheet silicates Fe or sheet silicates (FeSS) extracted with boiling 12 M HCl; (3) Reducible oxyhydr(oxides), including goethite, akagenite and hematite Fe (Fe-oxy) with sodium dithionite, and magnetite Fe with ammonium oxalate (FeMag); (4) Carbonate-associated Fe (FeCarb) extracted with sodium acetate; (5) pyrite Fe (FePy) extracted using the chromium reduction method. (6) Unreactive silicate Fe (FeURS) was determined as FeURS = (FeT) - (FeSS + Fe-oxy + FeMag + FeCarb + FePy).

## Chemically extractable Fe-bound P analysis

Co-extracted P associated with the Fe phases was approximated following the optimized Fe-P speciation extraction procedure of Thompson and others⁴⁰ for ancient sediments and Fe and P co-measured by ICP-AES. These included Fe carbonate bound-P (Fe-Pcarb), Fe oxyhydr(-oxides) associated-P (Fe-oxHR-P), magnetite bound-P (PMag) and sheet silicate Fe associated P (PSS). The remaining P was assumed tied up mainly with unreactive silicates (PURS), first verified by a lack of correlation between total organic carbon and P. We use multiple lines of geochemical evidence, together with Loss on Ignition (LOI) to show that most P trapped in the sediments is bound to inorganic mineral phases. Further, SEM-EDS and XRD analyses were used to show that apatite is not a major mineral phase in the sediments. The potential PURS fraction was then estimated from PURS = (PT) - (Fe-Pcarb + Fe-oxHR-P + PMag + PSS). Because of the linear correlation between dissolved P and particulate Fe-oxHR in marine sediments³⁷⁻³⁹, we further evaluate the distribution of P in the Fe-oxHR phases to approximate the general behaviour of dissolved P across the studied section.

## Stable isotope analysis

For analysis of δ¹³C and δ¹⁸O in carbonates, powdered samples weighed into septum vials were flushed with helium, acidified with 99% orthophosphoric acid, and left to react for 24 hours at 60 °C to ensure complete dolomite dissolution. The long-term precision of in-house Carrara marble standard was 0.05‰ for both δ¹⁸O and δ¹³C (1 SD). Organic carbon samples were acidified in 10% HCl and left to react for up to two days to remove all inorganic carbon, prior to δ¹³Corg measurement. Residues were rinsed three times, dried and weighed into tin capsules. The aperture of the autosampler determined the maximum amount of sediment that could be analysed for Corg to be 60-80 mg. Because of low Corg content, total analysable minimum Corg was estimated to be 10 µg. To allow calibration of such small samples, three standards (IAEA-CH6 [δ¹³C = −10.449], IAEA-600 [δ¹³C = −27.771] and in-house caffeine [δ¹³C = −33.30]) were dissolved in de-ionised water to improve homogeneity and allow accurate dosing of small aliquots using a micropipette. Results for IAEA-CH6 and the in-house caffeine were used to estimate a correction function for sample size and size-dependent two-point normalization, which was applied to IAEA-600 as independent standard. The resultant precision was dependent on sample size. The long-term precision for δ¹³C was estimated to be 0.09 (1 SD) for routine samples containing ≥100 µg C. However, the standard deviation increases with decreasing sample size to 0.38 for aliquots of 10–30 µg C for the present study (IAEA-600, n = 15). Iron isotope analysis was conducted on rock powders as previously described⁷¹.

## Numerical modelling

A four-box ocean PO₄³⁻ model was simulated using the equations described in reference⁶⁴. The model was operated from an initial low oxygen steady state and followed by a pulse of reactive P from a
<figure><img src="image_18.png" /><figcaption>**Fig. 9 |** A conceptual model for P cycling across the Sturtian Snowball glaciation. The model highlights the relationship between glacially generated clays, P and Fe.</figcaption></figure>

samples along sequence stratigraphy. Prior to geochemical analysis, the outer exposed layers of samples were removed and only the unweathered portions were used for analysis. A fraction was milled into a fine powder for geochemical, chemostratigraphic and XRD mineralogical analyses. Slices of whole rock samples were thin sectioned and polished for scanning electron microscopy-energy dispersive spectroscopy (SEM-EDS).

## Mineralogical analysis

X-ray diffraction (XRD) analysis for bulk semi-quantitative qualitative mineralogy analysis was undertaken with a PANalytical Xpert-pro and a Bruker D8 ADVANCE diffractometers at Cardiff University and University of Poitiers, respectively, as previously described⁶⁹⁻⁷¹. SEM-EDS analysis was performed with an Oxford FEI-XL30 fitted Environmental SEM (ESEM) connected to an EDS system at Cardiff University. Analyses were conducted on polished thin sections coated with carbon to a thickness of 14 nm with a BIO-RAD SC500 sputter. The SEM-EDS analyses were run at a working distance of 8.9 mm and a 15 kV accelerating voltage. Backscattered elemental maps, point-specific atomic composition and spectra were combined to identify putative mineral phases. Semi-quantitative XRD analyses of the relative abundance of the mineral assemblages was calculated using the integrated area ratios of the principal peaks after decomposition by the FYTIK program⁷².

## Elemental analysis

An approximate 250 mg of bulk rock powders were dissolved using reagent grade acids in closed screw-top Teflon vessels (Savillex) at 90 °C for one day in concentrated 3 ml 40% HF, 3 ml 32% HCl, and 1 ml 65% HNO₃. Excess HF was neutralised with 93 ml H₃BO₃ (20 g/L) aqueous solution. Elements were measured by inductively coupled plasma atomic emission spectrometry (ICP-AES) using a Horiba Jobin Yvon® Ultima 2 spectrometer with boron as an internal standard. Calibrations were made with ACE, JB2, and WSE international standards, with relative standard deviation of ≤1% for SiO₂, ≤2% for the other major elements, and ≤5% for traces elements.

## Iron speciation analysis

Chemical extraction of sediment Fe phases was conducted using the sequential Fe extraction protocol of Poulton and Canfield and Fe measured using the ferrozine method³⁴⁻³⁶. Redox trends were further constrained using the distribution of Fe/Al ratios across the studied

section, where average ratios of ~0.55 ± 0.11 are common for oxic waters, with much greater values for anoxic settings³⁴⁻³⁶. Sediment Al/ (Al+Fe+Mn) content was used to demonstrate that hydrothermal contribution²⁵ of Fe to the sediments was negligible and that observed high Fe/Al ratios cannot be associated with hydrothermal activity. The sequential Fe extraction procedure resulted in the quantification of eight operationally defined Fe phases: (1) Total bulk rock Fe (FeT) from whole rock dissolved powder using hydrofluoric acid (HF); (2) Poorly reactive sheet silicates Fe or sheet silicates (FeSS) extracted with boiling 12 M HCl; (3) Reducible oxyhydr(oxides), including goethite, akagenite and hematite Fe (Fe-oxy) with sodium dithionite, and magnetite Fe with ammonium oxalate (FeMag); (4) Carbonate-associated Fe (FeCarb) extracted with sodium acetate; (5) pyrite Fe (FePy) extracted using the chromium reduction method. (6) Unreactive silicate Fe (FeURS) was determined as FeURS = (FeT) - (FeSS + Fe-oxy + FeMag + FeCarb + FePy).

## Chemically extractable Fe-bound P analysis

Co-extracted P associated with the Fe phases was approximated following the optimized Fe-P speciation extraction procedure of Thompson and others⁴⁰ for ancient sediments and Fe and P co-measured by ICP-AES. These included Fe carbonate bound-P (Fe-Pcarb), Fe oxyhydr(-oxides) associated-P (Fe-oxHR-P), magnetite bound-P (PMag) and sheet silicate Fe associated P (PSS). The remaining P was assumed tied up mainly with unreactive silicates (PURS), first verified by a lack of correlation between total organic carbon and P. We use multiple lines of geochemical evidence, together with Loss on Ignition (LOI) to show that most P trapped in the sediments is bound to inorganic mineral phases. Further, SEM-EDS and XRD analyses were used to show that apatite is not a major mineral phase in the sediments. The potential PURS fraction was then estimated from PURS = (PT) - (Fe-Pcarb + Fe-oxHR-P + PMag + PSS). Because of the linear correlation between dissolved P and particulate Fe-oxHR in marine sediments³⁷⁻³⁹, we further evaluate the distribution of P in the Fe-oxHR phases to approximate the general behaviour of dissolved P across the studied section.

## Stable isotope analysis

For analysis of δ¹³C and δ¹⁸O in carbonates, powdered samples weighed into septum vials were flushed with helium, acidified with 99% orthophosphoric acid, and left to react for 24 hours at 60 °C to ensure complete dolomite dissolution. The long-term precision of in-house Carrara marble standard was 0.05‰ for both δ¹⁸O and δ¹³C (1 SD). Organic carbon samples were acidified in 10% HCl and left to react for up to two days to remove all inorganic carbon, prior to δ¹³Corg measurement. Residues were rinsed three times, dried and weighed into tin capsules. The aperture of the autosampler determined the maximum amount of sediment that could be analysed for Corg to be 60-80 mg. Because of low Corg content, total analysable minimum Corg was estimated to be 10 µg. To allow calibration of such small samples, three standards (IAEA-CH6 [δ¹³C = −10.449], IAEA-600 [δ¹³C = −27.771] and in-house caffeine [δ¹³C = −33.30]) were dissolved in de-ionised water to improve homogeneity and allow accurate dosing of small aliquots using a micropipette. Results for IAEA-CH6 and the in-house caffeine were used to estimate a correction function for sample size and size-dependent two-point normalization, which was applied to IAEA-600 as independent standard. The resultant precision was dependent on sample size. The long-term precision for δ¹³C was estimated to be 0.09 (1 SD) for routine samples containing ≥100 µg C. However, the standard deviation increases with decreasing sample size to 0.38 for aliquots of 10–30 µg C for the present study (IAEA-600, n = 15). Iron isotope analysis was conducted on rock powders as previously described⁷¹.

## Numerical modelling

A four-box ocean PO₄³⁻ model was simulated using the equations described in reference⁶⁴. The model was operated from an initial low oxygen steady state and followed by a pulse of reactive P from a
riverine source or from within the ocean. The latter state represents within the ocean the chemical weathering of glacial debris as a source of PO₄³⁻ to seawater. The initial steady state flux conditions at t = 0 assume half the annual amount of current riverine PO₄³⁻ supply to seawater and increased flux of reductants to the surface ocean equivalent to 1×10¹³ mol O₂, equating to ~5% PAL of O₂ producing a slightly oxic ocean surface and anoxic ocean interior and shelf bottom waters, except for ~20% of the proximal shelf. At t = 0 a pulse of P was delivered to the system by increasing the riverine PO₄³⁻ input by 50% for a total of 5 Myr in duration or adding this additional PO₄³⁻ throughout the ocean interior. In agreement with geological evidence, the model calculates the relationship between PO₄³⁻ and ocean-atmosphere oxygenation and PO₄³⁻ burial rates as authigenic calcium phosphate, Fe-oxHR and organic matter bound P (refs. 64,65).

## Data availability

All data are available in the supplementary information and supplementary Data 1-6.

## References

1. Planavsky, N. J. et al. The evolution of the marine phosphate reservoir. *Nature* **467**, 1088-1090 (2010).

2. Reinhard, C. T. et al. Evolution of the global phosphate cycle. *Nature* **541**, 386-389 (2017).

3. Lyons, T. W., Reinhard, C. T. & Planavsky, N. J. The rise of oxygen in Earth's early ocean and atmosphere. *Nature* **506**, 307-315 (2014).

4. Gerard, F. Clay minerals, iron/aluminium oxides, and their contribution to phosphate adsorption in soils — a myth revisited. *Geoderma* **262**, 213-226 (2016).

5. Hao, W. et al. The kaolinite shuttle: A mechanistic link between the Great Oxidation Event and Earth's largest carbon burial event. *Nat. Comm.* **12**, 2944 (2021).

6. Froelich, P. N. Kinetic control of dissolved phosphate in natural rivers and estuaries: a primer on the phosphate buffer mechanism. *1. Limnol. Oceanogr.* **33**, 649-668 (1988).

7. Hoffman, P. F. et al. Snowball Earth climate dynamics and Cryogenian geology-geobiology. *Sci. Adv.* **3**, e1600983 (2017).

8. Hawking, J. et al. The Greenland ice sheet as a hot spot of phosphorus weathering and export in the Arctic. *Glob. Biogeochem. Cycles* **30**, 191-210 (2015).

9. Mavris, C. et al. Clay mineral evolution along a soil chronosequence in an Alpine proglacial area. *Geoderma* **165**, 106-117 (2011).

10. Violante, A. & Pigna, M. Competitive sorption of arsenate and phosphate on different clay minerals and soils. *Soil Sci. Soc. Am. J.* **66**, 1788-1796 (2002).

11. Némery, J. & Garnier, J. The typical features of particulate phosphorus in the Seine Estuary (France). *Hydrobiologia* **588**, 271-290 (2007).

12. Ajmal, Z. et al. Phosphate removal from aqueous solution using iron oxides: adsorption, desorption and regeneration characteristics. *J. Colloid Inter. Sci.* **528**, 145-155 (2018).

13. Daou, T. J. et al. Phosphate adsorption properties of magnetite-based nanoparticles. *Chem. Mat.* **19**, 4494-4505 (2007).

14. Kim, J., Li, W., Philips, B. L. & Grey, C. P. Phosphate adsorption on the iron oxyhydroxides goethite (a-FeOOH), akaganeite (b-FeOOH), and lepidocrocite (g-FeOOH): a ¹³P NMR Study. *Energy Environ. Sci.* **4**, 4298 (2011).

15. Liu, J. et al. Adsorption of phosphate and cadmium on iron (oxyhydr) oxides: A comparative study on ferrihydrite, goethite, and hematite. *Geoderma* **383**, 114799 (2021).

16. Liang, X. et al. Competitive adsorption geometries for the arsenate As(V) and phosphate P(V) oxyanions on magnetite surfaces: Experiments and theory. *Am. Min.* **106**, 374-388 (2021).

17. Warr, L. N. Earth's clay mineral inventory and its climate interaction: A quantitative assessment. *Earth-Sci. Rev.* **234**, 104198 (2022).

18. Arnaud, E. & Fairchild, I. J. The Port Askaig Formation, Dalradian Supergroup, Scotland. *Geol. Soc. Lond. Mem.* **36**, 635-642 (2011).

19. Brasier, M. D. & Shields, G. Neoproterozoic chemostratigraphy and correlation of the Port Askaig glaciation, Dalradian Supergroup of Scotland. *J. Geol. Soc. Lond.* **157**, 909-914 (2000).

20. Thomas, C. W., Graham, C. M., Ellam, R. M. & Fallick, A. E. ⁸⁷Sr/⁸⁶Sr chemostratigraphy of Neoproterozoic Dalradian limestones of Scotland and Ireland: constraints on depositional ages and time scales. *J. Geol. Soc. Lond.* **161**, 229-242 (2004).

21. Fairchild, I. J. et al. Tonian-Cryogenian boundary sections of Argyll, Scotland. *Pre. Res.* **319**, 37-64 (2018).

22. Prave, T., Fallick, A. E., Thomas, C. W. & Graham, C. M. A composite C-isotope profile for the Neoproterozoic Dalradian Supergroup of Scotland and Ireland. *J. Geol. Soc.* **166**, 845-857 (2009).

23. Sawaki, Y. et al. ⁸⁷Sr/⁸⁶Sr chemostratigraphy of Neoproterozoic Dalradian carbonates below the Port Askaig Glaciogenic Formation, Scotland. *Pre. Res.* **179**, 150-164 (2010).

24. Skelton, A. D. L., Valley, J. V., Graham, C. M., Bickle, M. J. & Fallick, A. E. The correlation of reaction and isotope fronts and the mechanism of metamorphic fluid flow. *Contrib. Min. Petrol.* **138**, 364-375 (2000).

25. Pecoits, E. et al. Petrography and geochemistry of the Dales Gorge banded iron formation: Paragenetic sequence, source and implications for palaeo-ocean chemistry. *Pre. Res.* **172**, 163-187 (2009).

26. Galan E. Genesis of clay minerals. In handbook of clay science (Edited by F. Bergaya, B. K. G. Theng and G. Lagaly. Developments in Clay Science, Vol. 1 Elsevier Ltd (2006).

27. Konhauser, K. O. et al. Aerobic bacteria pyrite oxidation and acid rock drainage during the Great Oxidation Event. *Nature* **478**, 369-373 (2011).

28. Chi Fru, E. et al. The rise of oxygen-driven arsenic cycling at ca. 2.48 Ga. *Geology* **47**, 243-246 (2019).

29. Heiri, O., Lotter, A. F. & Lemcke, G. Loss on ignition as a method for estimating organic and carbonate content in sediments: reproducibility and comparability of result. *J. Paleolim.* **25**, 101-110 (2015).

30. Ruttenberg, K. & Berner, R. A. Authigenic apatite formation and burial in sediments from non-upwelling, continental margin environments. *Geochim. Cosmo. Acta* **57**, 991-1007 (1993).

31. Dodd, M. S. et al. Development of carbonate-associated phosphate (CAP) as a proxy for reconstructing ancient ocean phosphate levels. *Geochim. Cosmo. Acta* **301**, 46-68 (2021).

32. Akcil, A. & Koldas, S. Acid Mine Drainage (AMD): causes, treatment and case studies. *J. Clean. Prod.* **14**, 1139-1144 (2006).

33. Panahi, A. & Young, G. M. A geochemical investigation into the provenance of the Neoproterozoic Port Askaig Tillite, Dalradian Supergroup, western Scotland. *Pre. Res.* **85**, 81-96 (1997).

34. Raiswell, R. et al. The iron paleoredox proxies: A guide to the pitfalls, problems and proper practice. *Am. J. Sci.* **318**, 491-526 (2018).

35. Poulton, S. W. & Canfield, D. E. Development of a sequential extraction procedure for iron: Implications for iron partitioning in continentally derived particulates. *Chem. Geol.* **214**, 209-221 (2005).

36. Poulton, S. W. & Canfield, D. E. Ferruginous conditions: A dominant feature of the ocean through Earth's history. *Elements* **7**, 107-112 (2011).

37. Feely, R. A., Trefry, J. H., Lebon, G. T. & German, C. R. The relationship between P/Fe and V/Fe ratios in hydrothermal precipitates and dissolved phosphate in seawater. *Geophys. Res. Lett.* **25**, 2253-2256 (1998).

38. Bjerrum, C. J. & Canfield, D. E. Ocean productivity before about 1.9 Gyr ago limited by phosphorus adsorption onto iron oxides. *Nature* **417**, 159-162 (2002).

39. Wheat, C. G., Feely, R. A. & Mottl, M. J. Phosphate removal by oceanic hydrothermal processes: An update of the phosphorus budget in the oceans. *Geochim. Cosmo. Acta* **60**, 3593-3608 (1996).
riverine source or from within the ocean. The latter state represents within the ocean the chemical weathering of glacial debris as a source of PO₄³⁻ to seawater. The initial steady state flux conditions at t = 0 assume half the annual amount of current riverine PO₄³⁻ supply to seawater and increased flux of reductants to the surface ocean equivalent to 1×10¹³ mol O₂, equating to ~5% PAL of O₂ producing a slightly oxic ocean surface and anoxic ocean interior and shelf bottom waters, except for ~20% of the proximal shelf. At t = 0 a pulse of P was delivered to the system by increasing the riverine PO₄³⁻ input by 50% for a total of 5 Myr in duration or adding this additional PO₄³⁻ throughout the ocean interior. In agreement with geological evidence, the model calculates the relationship between PO₄³⁻ and ocean-atmosphere oxygenation and PO₄³⁻ burial rates as authigenic calcium phosphate, Fe-oxHR and organic matter bound P (refs. 64,65).

## Data availability

All data are available in the supplementary information and supplementary Data 1-6.

## References

1. Planavsky, N. J. et al. The evolution of the marine phosphate reservoir. *Nature* **467**, 1088-1090 (2010).

2. Reinhard, C. T. et al. Evolution of the global phosphate cycle. *Nature* **541**, 386-389 (2017).

3. Lyons, T. W., Reinhard, C. T. & Planavsky, N. J. The rise of oxygen in Earth's early ocean and atmosphere. *Nature* **506**, 307-315 (2014).

4. Gerard, F. Clay minerals, iron/aluminium oxides, and their contribution to phosphate adsorption in soils — a myth revisited. *Geoderma* **262**, 213-226 (2016).

5. Hao, W. et al. The kaolinite shuttle: A mechanistic link between the Great Oxidation Event and Earth's largest carbon burial event. *Nat. Comm.* **12**, 2944 (2021).

6. Froelich, P. N. Kinetic control of dissolved phosphate in natural rivers and estuaries: a primer on the phosphate buffer mechanism. *1. Limnol. Oceanogr.* **33**, 649-668 (1988).

7. Hoffman, P. F. et al. Snowball Earth climate dynamics and Cryogenian geology-geobiology. *Sci. Adv.* **3**, e1600983 (2017).

8. Hawking, J. et al. The Greenland ice sheet as a hot spot of phosphorus weathering and export in the Arctic. *Glob. Biogeochem. Cycles* **30**, 191-210 (2015).

9. Mavris, C. et al. Clay mineral evolution along a soil chronosequence in an Alpine proglacial area. *Geoderma* **165**, 106-117 (2011).

10. Violante, A. & Pigna, M. Competitive sorption of arsenate and phosphate on different clay minerals and soils. *Soil Sci. Soc. Am. J.* **66**, 1788-1796 (2002).

11. Némery, J. & Garnier, J. The typical features of particulate phosphorus in the Seine Estuary (France). *Hydrobiologia* **588**, 271-290 (2007).

12. Ajmal, Z. et al. Phosphate removal from aqueous solution using iron oxides: adsorption, desorption and regeneration characteristics. *J. Colloid Inter. Sci.* **528**, 145-155 (2018).

13. Daou, T. J. et al. Phosphate adsorption properties of magnetite-based nanoparticles. *Chem. Mat.* **19**, 4494-4505 (2007).

14. Kim, J., Li, W., Philips, B. L. & Grey, C. P. Phosphate adsorption on the iron oxyhydroxides goethite (a-FeOOH), akaganeite (b-FeOOH), and lepidocrocite (g-FeOOH): a ¹³P NMR Study. *Energy Environ. Sci.* **4**, 4298 (2011).

15. Liu, J. et al. Adsorption of phosphate and cadmium on iron (oxyhydr) oxides: A comparative study on ferrihydrite, goethite, and hematite. *Geoderma* **383**, 114799 (2021).

16. Liang, X. et al. Competitive adsorption geometries for the arsenate As(V) and phosphate P(V) oxyanions on magnetite surfaces: Experiments and theory. *Am. Min.* **106**, 374-388 (2021).

17. Warr, L. N. Earth's clay mineral inventory and its climate interaction: A quantitative assessment. *Earth-Sci. Rev.* **234**, 104198 (2022).

18. Arnaud, E. & Fairchild, I. J. The Port Askaig Formation, Dalradian Supergroup, Scotland. *Geol. Soc. Lond. Mem.* **36**, 635-642 (2011).

19. Brasier, M. D. & Shields, G. Neoproterozoic chemostratigraphy and correlation of the Port Askaig glaciation, Dalradian Supergroup of Scotland. *J. Geol. Soc. Lond.* **157**, 909-914 (2000).

20. Thomas, C. W., Graham, C. M., Ellam, R. M. & Fallick, A. E. ⁸⁷Sr/⁸⁶Sr chemostratigraphy of Neoproterozoic Dalradian limestones of Scotland and Ireland: constraints on depositional ages and time scales. *J. Geol. Soc. Lond.* **161**, 229-242 (2004).

21. Fairchild, I. J. et al. Tonian-Cryogenian boundary sections of Argyll, Scotland. *Pre. Res.* **319**, 37-64 (2018).

22. Prave, T., Fallick, A. E., Thomas, C. W. & Graham, C. M. A composite C-isotope profile for the Neoproterozoic Dalradian Supergroup of Scotland and Ireland. *J. Geol. Soc.* **166**, 845-857 (2009).

23. Sawaki, Y. et al. ⁸⁷Sr/⁸⁶Sr chemostratigraphy of Neoproterozoic Dalradian carbonates below the Port Askaig Glaciogenic Formation, Scotland. *Pre. Res.* **179**, 150-164 (2010).

24. Skelton, A. D. L., Valley, J. V., Graham, C. M., Bickle, M. J. & Fallick, A. E. The correlation of reaction and isotope fronts and the mechanism of metamorphic fluid flow. *Contrib. Min. Petrol.* **138**, 364-375 (2000).

25. Pecoits, E. et al. Petrography and geochemistry of the Dales Gorge banded iron formation: Paragenetic sequence, source and implications for palaeo-ocean chemistry. *Pre. Res.* **172**, 163-187 (2009).

26. Galan E. Genesis of clay minerals. In handbook of clay science (Edited by F. Bergaya, B. K. G. Theng and G. Lagaly. Developments in Clay Science, Vol. 1 Elsevier Ltd (2006).

27. Konhauser, K. O. et al. Aerobic bacteria pyrite oxidation and acid rock drainage during the Great Oxidation Event. *Nature* **478**, 369-373 (2011).

28. Chi Fru, E. et al. The rise of oxygen-driven arsenic cycling at ca. 2.48 Ga. *Geology* **47**, 243-246 (2019).

29. Heiri, O., Lotter, A. F. & Lemcke, G. Loss on ignition as a method for estimating organic and carbonate content in sediments: reproducibility and comparability of result. *J. Paleolim.* **25**, 101-110 (2015).

30. Ruttenberg, K. & Berner, R. A. Authigenic apatite formation and burial in sediments from non-upwelling, continental margin environments. *Geochim. Cosmo. Acta* **57**, 991-1007 (1993).

31. Dodd, M. S. et al. Development of carbonate-associated phosphate (CAP) as a proxy for reconstructing ancient ocean phosphate levels. *Geochim. Cosmo. Acta* **301**, 46-68 (2021).

32. Akcil, A. & Koldas, S. Acid Mine Drainage (AMD): causes, treatment and case studies. *J. Clean. Prod.* **14**, 1139-1144 (2006).

33. Panahi, A. & Young, G. M. A geochemical investigation into the provenance of the Neoproterozoic Port Askaig Tillite, Dalradian Supergroup, western Scotland. *Pre. Res.* **85**, 81-96 (1997).

34. Raiswell, R. et al. The iron paleoredox proxies: A guide to the pitfalls, problems and proper practice. *Am. J. Sci.* **318**, 491-526 (2018).

35. Poulton, S. W. & Canfield, D. E. Development of a sequential extraction procedure for iron: Implications for iron partitioning in continentally derived particulates. *Chem. Geol.* **214**, 209-221 (2005).

36. Poulton, S. W. & Canfield, D. E. Ferruginous conditions: A dominant feature of the ocean through Earth's history. *Elements* **7**, 107-112 (2011).

37. Feely, R. A., Trefry, J. H., Lebon, G. T. & German, C. R. The relationship between P/Fe and V/Fe ratios in hydrothermal precipitates and dissolved phosphate in seawater. *Geophys. Res. Lett.* **25**, 2253-2256 (1998).

38. Bjerrum, C. J. & Canfield, D. E. Ocean productivity before about 1.9 Gyr ago limited by phosphorus adsorption onto iron oxides. *Nature* **417**, 159-162 (2002).

39. Wheat, C. G., Feely, R. A. & Mottl, M. J. Phosphate removal by oceanic hydrothermal processes: An update of the phosphorus budget in the oceans. *Geochim. Cosmo. Acta* **60**, 3593-3608 (1996).
40. Thompson, J. et al. Development of a modified SEDEX phosphorus speciation method for ancient rocks and modern iron-rich sediments. *Chem. Geol.* **524**, 383–395 (2019).

41. Lyons, T. W. & Severman, S. A critical look at iron paleoredox proxies: New insights from modern euoxic marine basins. *Geo-chim. Cosmo. Acta* **70**, 5698–5722 (2006).

42. Lyons, T. W., Werne, J. P., Hollander, D. J. & Murray, R. W. Contrasting sulfur geochemistry and Fe/Al and Mo/Al ratios across the last oxic-to-anoxic transition in the Cariaco Basin, Venezuela. *Chem. Geol.* **195**, 131–157 (2003).

43. Hepburn, L. E., Butler, I. B., Boyce, A. & Schröder, C. The use of operationally-defined sequential Fe extraction methods for mineralogical applications: A cautionary tale from Mössbauer spectroscopy. *Chem. Geol.* **543**, 119584 (2020).

44. Han, Z. et al. Using Zn and Ni behavior during magnetite precipitation in banded iron formations to determine its biological or abiotic origin. *Earth Plan. Sci. Letts.* **568**, 117052 (2022).

45. Halama, M., Swanner, E. D., Konhauser, K. O. & Kappler, A. Evaluation of siderite and magnetite formation in BIFs by pressure-temperature experiments of Fe(III) minerals and microbial biomass. *Earth Planet. Sci. Lett.* **450**, 243–253 (2016).

46. Halevy, I., Alesker, M., Schuster, E. M., Popovitzbiro, R. & Feldman, Y. A key role for green rust in the Precambrian oceans and the genesis of iron formations. *Nat. Geosci.* **10**, 135–139 (2017).

47. Han, X. et al. Effect of microbial biomass and humic acids on abiotic and biotic magnetite formation. *Environ. Sci. Technol.* **54**, 4121–4130 (2020).

48. Konhauser, K. O., Newman, D. K. & Kappler, A. The potential significance of microbial Fe(III) reduction during deposition of Precambrian banded iron formations. *Geobiology* **3**, 167–177 (2005).

49. Zegeye, A. et al. Green rust formation controls nutrient availability in a ferruginous water column. *Geology* **40**, 599–602 (2012).

50. Hansen, C. R. H. & Poulsen, I. F. Interaction of synthetic sulphate "green rust" with phosphate and the crystallization of vivianite. *Clays Clay Miner.* **47**, 312–318 (1999).

51. Chi Fru, E., Hemmingsson, C., Holm, M., Chiu, B. & Iñiguez, E. Arsenic-induced phosphate limitation under experimental Early Proterozoic oceanic conditions. *Earth Plan. Sci. Lett.* **434**, 52–63 (2016).

52. Hemmingsson, C., Pitcairn, I. & Chi Fru, E. Evaluation of phosphate-uptake mechanisms by Fe(III) (oxyhydr)oxides in Early Proterozoic oceanic conditions. *Environ. Chem.* **15**, 18–28 (2018).

53. Barthélémy, K., Naille, S., Despas, C., Ruby, C. & Mallet, M. Carbonated ferric green rust as a new material for efficient phosphate removal. *J. Colloid Interface Sci.* **384**, 121–127 (2012).

54. Konhauser, K. O., Lalonde, S., Amskold, L. & Holland, H. D. Was there really an Archean phosphate crisis? *Science* **315**, 1234 (2007).

55. Frost, C. D., von Blanckenburg, F., Schoenberg, R., Frost, B. R. & Swapp, S. M. Preservation of Fe isotope heterogeneities during diagenesis and metamorphism of banded iron formation. *Contrib. Miner. Petrol.* **153**, 211–235 (2007).

56. Klein, C. Some Precambrian banded iron-formations (BIFs) from around the world: their age, geologic setting, mineralogy, metamorphism, geochemistry, and origins. *Am. Miner.* **90**, 1473 (2005).

57. Rasmussen, B. & Muhling, J. R. Making magnetite late again: evidence for widespread magnetite growth by thermal decomposition of siderite in Hamersley banded iron formations. *Pre. Res.* **306**, 64–93 (2018).

58. Hopwood, M. J. et al. Review article: How does glacier discharge affect marine biogeochemistry and primary production in the Arctic? *Cryosphere* **14**, 1347–1383 (2020).

59. Boyle, E. A., Edmond, J. M. & Sholkovitz, E. R. Mechanism of iron removal in estuaries, 1477. *Geochim. Cosmochim. Acta* **4**, 1313–1324 (1977).

60. Planavsky, N. et al. Iron isotope composition of some Archean and Proterozoic iron formations. *Geochim. Cosmochim. Acta* **80**, 158–169 (2012).

61. Gnanaprakash, G. et al. Effect of initial pH and temperature of iron salt solutions on formation of magnetite nanoparticles. *Mat. Chem. Phy.* **103**, 168–175 (2007).

62. Pang, S. C., Chin, S. F. & Anderson, M. A. Redox equilibria of iron oxides in aqueous-based magnetite dispersions: Effect of pH and redox potential. *J. Colloid Inter. Sci.* **311**, 94–101 (2007).

63. Clarkson, M. O., Poulton, S. W., Guilbaud, R. & Wood, R. A. Assessing the utility of Fe/Al and Fe-speciation to record water column redox conditions in carbonate-rich sediments. *Chem. Geol.* **382**, 111–122 (2014).

64. Alcott, L. J., Mills, J. W. & Poulton, S. W. Stepwise Earth oxygenation is an inherent property of global biogeochemical cycling. *Science* **6471**, 1333–1337 (2019).

65. Slomp, C. P. & Van Cappellen, P. The global marine phosphorus cycle: sensitivity to the oceanic circulation. *Biogeosciences* **4**, 155–171 (2007).

66. Macdonald, M. L., Wadham, J. L., Telling, J. & Skidmore, M. L. Glacial erosion liberates lithologic energy sources for microbes and acidity for chemical weathering beneath glaciers and ice sheets. *Front. Earth Sci.* **6**, 212 (2018).

67. Huang, K. J. et al. Episode of intense chemical weathering during the termination of the 635 Ma Marinoan glaciation. *Proc. Natl Acad. Sci. USA.* **113**, 14904–14909 (2016).

68. Smith, E. A., Mayfield, C. I. & Wong, P. T. S. Physical and chemical characterization of selected natural apatites in synthetic and natural aqueous solutions. *Water Air Soil Pollut.* **8**, 401–415 (1977).

69. Moore D. M., Reynolds Jr R. C. X-Ray Diffraction and the Identification and Analysis of Clay Minerals, 2nd edition. Oxford University Press, New York. (1997).

70. Johns, W. D., Grim, R. E. & Bradley, W. F. Quantitative estimations of clay minerals by diffraction methods. *J. Sed. Petrol.* **24**, 242–251 (1954).

71. Chi Fru, E. et al. Early Neoproterozoic oxygenation dynamics along the northern margin of the West African Craton, Anti-Atlas Mountains, Morocco. *Chem. Geol.* **581**, 120404 (2021).

72. Wojdyr, M. Fityk: a general-purpose peak fitting program. *J. Appl. Crystallogr.* **43**, 1126–1128 (2010).

73. Tribovillard, N., Algeo, T. J., Lyons, T. & Riboulleau, A. Trace metals as paleoredox and paleoproductivity proxies: An update. *Chem. Geol.* **232**, 12–32 (2006).

74. Rudnick R. L. & Gao S. Composition of the continental crust. In The Crust, vol. 3 (ed. Rudnick R. L.). Elsevier, 1-64 (2003).

## Acknowledgements

Thanks to Diana Carlsson for help with the fieldwork and sample collection, Stefan Lalonde with trace and major element analyses and Olivier Rouxel for support with iron isotope analysis. We are grateful to Ian Fairchild for inspiring important discussions on the Cryogenian sedimentology and stratigraphy of Islay and the Garvellachs Islands. We thank Flavia Boscolo Galazzo for insightful comments. This work was supported by funds from The European Research Council (ERC) Seventh Framework (F7) program, grant No: 336092. Support is acknowledged from La Région Nouvelle Aquitaine, France.

## Author contributions

E.C.F. designed research; E.C.F., C.B., A.O., A.N., O.B., J.A.B. and J.A. conducted research; L.A. and B.M. developed the numerical model; D.W. and A.S. produced field and stratigraphic maps. E.C.F. and L.L. collected samples; E.C.F., A.E., K.K., O.B., W.F., J.A.B., J.A. and T.L. analysed data. E.C.F. wrote the paper with significant contributions from all co-authors.
40. Thompson, J. et al. Development of a modified SEDEX phosphorus speciation method for ancient rocks and modern iron-rich sediments. *Chem. Geol.* **524**, 383–395 (2019).

41. Lyons, T. W. & Severman, S. A critical look at iron paleoredox proxies: New insights from modern euxinic marine basins. *Geo-chim. Cosmo. Acta* **70**, 5698–5722 (2006).

42. Lyons, T. W., Werne, J. P., Hollander, D. J. & Murray, R. W. Contrasting sulfur geochemistry and Fe/Al and Mo/Al ratios across the last oxic-to-anoxic transition in the Cariaco Basin, Venezuela. *Chem. Geol.* **195**, 131–157 (2003).

43. Hepburn, L. E., Butler, I. B., Boyce, A. & Schröder, C. The use of operationally-defined sequential Fe extraction methods for mineralogical applications: A cautionary tale from Mössbauer spectroscopy. *Chem. Geol.* **543**, 119584 (2020).

44. Han, Z. et al. Using Zn and Ni behavior during magnetite precipitation in banded iron formations to determine its biological or abiotic origin. *Earth Plan. Sci. Letts.* **568**, 117052 (2022).

45. Halama, M., Swanner, E. D., Konhauser, K. O. & Kappler, A. Evaluation of siderite and magnetite formation in BIFs by pressure-temperature experiments of Fe(III) minerals and microbial biomass. *Earth Planet. Sci. Lett.* **450**, 243–253 (2016).

46. Halevy, I., Alesker, M., Schuster, E. M., Popovitzbiro, R. & Feldman, Y. A key role for green rust in the Precambrian oceans and the genesis of iron formations. *Nat. Geosci.* **10**, 135–139 (2017).

47. Han, X. et al. Effect of microbial biomass and humic acids on abiotic and biotic magnetite formation. *Environ. Sci. Technol.* **54**, 4121–4130 (2020).

48. Konhauser, K. O., Newman, D. K. & Kappler, A. The potential significance of microbial Fe(III) reduction during deposition of Precambrian banded iron formations. *Geobiology* **3**, 167–177 (2005).

49. Zegeye, A. et al. Green rust formation controls nutrient availability in a ferruginous water column. *Geology* **40**, 599–602 (2012).

50. Hansen, C. R. H. & Poulsen, I. F. Interaction of synthetic sulphate “green rust” with phosphate and the crystallization of vivianite. *Clays Clay Miner.* **47**, 312–318 (1999).

51. Chi Fru, E., Hemmingsson, C., Holm, M., Chiu, B. & Iñiguez, E. Arsenic-induced phosphate limitation under experimental Early Proterozoic oceanic conditions. *Earth Plan. Sci. Lett.* **434**, 52–63 (2016).

52. Hemmingsson, C., Pitcairn, I. & Chi Fru, E. Evaluation of phosphate-uptake mechanisms by Fe(III) (oxyhydr)oxides in Early Proterozoic oceanic conditions. *Environ. Chem.* **15**, 18–28 (2018).

53. Barthélémy, K., Naille, S., Despas, C., Ruby, C. & Mallet, M. Carbonated ferric green rust as a new material for efficient phosphate removal. *J. Colloid Interface Sci.* **384**, 121–127 (2012).

54. Konhauser, K. O., Lalonde, S., Amskold, L. & Holland, H. D. Was there really an Archean phosphate crisis? *Science* **315**, 1234 (2007).

55. Frost, C. D., von Blanckenburg, F., Schoenberg, R., Frost, B. R. & Swapp, S. M. Preservation of Fe isotope heterogeneities during diagenesis and metamorphism of banded iron formation. *Contrib. Miner. Petrol.* **153**, 211–235 (2007).

56. Klein, C. Some Precambrian banded iron-formations (BIFs) from around the world: their age, geologic setting, mineralogy, metamorphism, geochemistry, and origins. *Am. Miner.* **90**, 1473 (2005).

57. Rasmussen, B. & Muhling, J. R. Making magnetite late again: evidence for widespread magnetite growth by thermal decomposition of siderite in Hamersley banded iron formations. *Pre. Res.* **306**, 64–93 (2018).

58. Hopwood, M. J. et al. Review article: How does glacier discharge affect marine biogeochemistry and primary production in the Arctic? *Cryosphere* **14**, 1347–1383 (2020).

59. Boyle, E. A., Edmond, J. M. & Sholkovitz, E. R. Mechanism of iron removal in estuaries, 1477. *Geochim. Cosmochim. Acta* **4**, 1313–1324 (1977).

60. Planavsky, N. et al. Iron isotope composition of some Archean and Proterozoic iron formations. *Geochim. Cosmochim. Acta* **80**, 158–169 (2012).

61. Gnanaprakash, G. et al. Effect of initial pH and temperature of iron salt solutions on formation of magnetite nanoparticles. *Mat. Chem. Phy.* **103**, 168–175 (2007).

62. Pang, S. C., Chin, S. F. & Anderson, M. A. Redox equilibria of iron oxides in aqueous-based magnetite dispersions: Effect of pH and redox potential. *J. Colloid Inter. Sci.* **311**, 94–101 (2007).

63. Clarkson, M. O., Poulton, S. W., Guilbaud, R. & Wood, R. A. Assessing the utility of Fe/Al and Fe-speciation to record water column redox conditions in carbonate-rich sediments. *Chem. Geol.* **382**, 111–122 (2014).

64. Alcott, L. J., Mills, J. W. & Poulton, S. W. Stepwise Earth oxygenation is an inherent property of global biogeochemical cycling. *Science* **6471**, 1333–1337 (2019).

65. Slomp, C. P. & Van Cappellen, P. The global marine phosphorus cycle: sensitivity to the oceanic circulation. *Biogeosciences* **4**, 155–171 (2007).

66. Macdonald, M. L., Wadham, J. L., Telling, J. & Skidmore, M. L. Glacial erosion liberates lithologic energy sources for microbes and acidity for chemical weathering beneath glaciers and ice sheets. *Front. Earth Sci.* **6**, 212 (2018).

67. Huang, K. J. et al. Episode of intense chemical weathering during the termination of the 635 Ma Marinoan glaciation. *Proc. Natl Acad. Sci. USA.* **113**, 14904–14909 (2016).

68. Smith, E. A., Mayfield, C. I. & Wong, P. T. S. Physical and chemical characterization of selected natural apatites in synthetic and natural aqueous solutions. *Water Air Soil Pollut.* **8**, 401–415 (1977).

69. Moore D. M., Reynolds Jr R. C. X-Ray Diffraction and the Identification and Analysis of Clay Minerals, 2nd edition. Oxford University Press, New York. (1997).

70. Johns, W. D., Grim, R. E. & Bradley, W. F. Quantitative estimations of clay minerals by diffraction methods. *J. Sed. Petrol.* **24**, 242–251 (1954).

71. Chi Fru, E. et al. Early Neoproterozoic oxygenation dynamics along the northern margin of the West African Craton, Anti-Atlas Mountains, Morocco. *Chem. Geol.* **581**, 120404 (2021).

72. Wojdyr, M. Fityk: a general-purpose peak fitting program. *J. Appl. Crystallogr.* **43**, 1126–1128 (2010).

73. Tribovillard, N., Algeo, T. J., Lyons, T. & Riboulleau, A. Trace metals as paleoredox and paleoproductivity proxies: An update. *Chem. Geol.* **232**, 12–32 (2006).

74. Rudnick R. L. & Gao S. Composition of the continental crust. In The Crust, vol. 3 (ed. Rudnick R. L.). Elsevier, 1–64 (2003).

## Acknowledgements

Thanks to Diana Carlsson for help with the fieldwork and sample collection, Stefan Lalonde with trace and major element analyses and Olivier Rouxel for support with iron isotope analysis. We are grateful to Ian Fairchild for inspiring important discussions on the Cryogenian sedimentology and stratigraphy of Islay and the Garvellachs Islands. We thank Flavia Boscolo Galazzo for insightful comments. This work was supported by funds from The European Research Council (ERC) Seventh Framework (F7) program, grant No: 336092. Support is acknowledged from La Région Nouvelle Aquitaine, France.

## Author contributions

E.C.F. designed research; E.C.F., C.B., A.O., A.N., O.B., J.A.B. and J.A. conducted research; L.A. and B.M. developed the numerical model; D.W. and A.S. produced field and stratigraphic maps. E.C.F. and L.L. collected samples; E.C.F., A.E., K.K., O.B., W.F., J.A.B., J.A. and T.L. analysed data. E.C.F. wrote the paper with significant contributions from all co-authors.
**Competing interests**

The authors declare no competing interests.

**Additional information**

**Supplementary information** The online version contains supplementary material available at https://doi.org/10.1038/s41467-023-44240-9.

**Correspondence** and requests for materials should be addressed to Ernest Chi Fru.

**Peer review information** *Nature Communications* thanks Weiduo Hao and Dominic Papineau for their contribution to the peer review of this work.

**Reprints and permissions information** is available at http://www.nature.com/reprints

**Publisher's note** Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.

**Open Access** This article is licensed under a Creative Commons Attribution 4.0 International License, which permits use, sharing, adaptation, distribution and reproduction in any medium or format, as long as you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made. The images or other third party material in this article are included in the article's Creative Commons license, unless indicated otherwise in a credit line to the material. If material is not included in the article's Creative Commons license and your intended use is not permitted by statutory regulation or exceeds the permitted use, you will need to obtain permission directly from the copyright holder. To view a copy of this license, visit http://creativecommons.org/licenses/by/4.0/.

© The Author(s) 2023
**Competing interests**

The authors declare no competing interests.

**Additional information**

**Supplementary information** The online version contains supplementary material available at https://doi.org/10.1038/s41467-023-44240-9.

**Correspondence** and requests for materials should be addressed to Ernest Chi Fru.

**Peer review information** *Nature Communications* thanks Weiduo Hao and Dominic Papineau for their contribution to the peer review of this work.

**Reprints and permissions information** is available at http://www.nature.com/reprints

**Publisher's note** Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.

**Open Access** This article is licensed under a Creative Commons Attribution 4.0 International License, which permits use, sharing, adaptation, distribution and reproduction in any medium or format, as long as you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made. The images or other third party material in this article are included in the article's Creative Commons license, unless indicated otherwise in a credit line to the material. If material is not included in the article's Creative Commons license and your intended use is not permitted by statutory regulation or exceeds the permitted use, you will need to obtain permission directly from the copyright holder. To view a copy of this license, visit http://creativecommons.org/licenses/by/4.0/.

© The Author(s) 2023