Skip to main content

Thank you for visiting You are using a browser version with limited support for CSS. To obtain the best experience, we recommend you use a more up to date browser (or turn off compatibility mode in Internet Explorer). In the meantime, to ensure continued support, we are displaying the site without styles and JavaScript.

UV radiation limited the expansion of cyanobacteria in early marine photic environments


Prior to atmospheric oxygenation, ecosystems were exposed to higher UV radiation fluxes relative to modern surface environments. Iron–silica mineral coatings have been evoked as effective UV radiation shields in early terrestrial settings. Here we test whether similar protection applied to planktonic cyanobacteria within the Archean water column. Based on experiments done under Archean seawater conditions, we report that Fe(III)–Si-rich precipitates absorb up to 70% of incoming UV-C radiation, with a reduction of <20% in photosynthetically active radiation flux. However, we demonstrate that even short periods of UV-C irradiation in the presence of Fe(III)–Si precipitates resulted in high mortality rates, and suggest that these effects would have persisted throughout much of the photic zone. Our findings imply that despite the shielding properties of Fe(III)–Si-rich precipitates in the early water column, UV radiation would continue to limit cyanobacterial expansion and likely had a greater effect on Archean ecosystem structure before the formation of an ozone layer.


Solar ultraviolet (UV) radiation is a key factor controlling the habitability of planetary surface environments and regulating the course of life’s evolution. Prior to 2.4 Ga and the development of a protective stratospheric ozone layer1, the flux of UV radiation—in particular UV-C wavelengths—reaching the surface of the Archean ocean was orders of magnitude higher than today2,3. As a result, rates of DNA damage to unprotected organisms could have limited the size and scope of the biosphere. In order to survive, photosynthesizing microorganisms, such as cyanobacteria, would have required either the evolution of DNA repair and protein turnover mechanisms to reverse the damage caused by UV radiation or an environmental mechanism to protect them against the harmful effects of radiation4. Additionally, renewed interest in the ability of life to tolerate high radiation environments has been sparked by the recent discovery of Earth-sized rocky planets within the habitable zones of a number of nearby M-dwarf stars (e.g., TRAPPIST-15, Proxima Centauri6, among others). These stars have substantially different stellar spectra compared to the sun, and the planets reside much closer to their stars, likely resulting in elevated UV radiation fluxes on these exoplanetary surfaces5,6. The results presented here highlight the importance of understanding environmental conditions on the early Earth as a case study to better quantify the potential for the emergence of substantial biospheres on exoplanetary surfaces likely to experience elevated UV radiation levels.

Modern cyanobacteria have mechanisms to counteract damage by UV radiation such as DNA excision repair and photoreactivation7, DNA repair systems like the SOS response8, detoxifying enzymes and pigments9, and UV radiation-absorbing sunscreen molecules10. However, these systems can rapidly become overwhelmed by sustained, high doses of UV radiation11, and some strains of cyanobacteria are often too small to accommodate enough sunscreen molecules for effective protection12. For benthic microorganisms, which live an aggregate lifestyle, mineralized coatings and extracellular sheaths provide physical protection from UV radiation13. Many of these organisms are able to migrate downward into the sediment or microbial mat and use exposure to UV radiation as an environmental cue14. While some planktonic cyanobacteria have the ability to adjust buoyancy by means of gas vacuoles or carbon ballasting15, regions of strong upwelling (where productivity will be highest) or wind-induced mixing within the upper tens of meters of the water column may still overcome those adjustments and force phototrophic bacteria seeking refuge within deeper parts of the photic zone to intermittent periods of exposure to high levels of UV radiation16.

Absorption of UV radiation in the oceans today occurs as a result of water’s optical and hydrodynamic properties as well as by dissolved and particulate matter suspended in the water column17. Within modern coastal habitats, plant-derived humic substances, either colored dissolved organic matter (CDOM) or particulate organic matter, play dominant roles in the attenuation of UV radiation18. Due in large part to the presence of CDOM in the water column, the diffuse attenuation coefficient of UV radiation for natural waters not only tends to vary greatly, but also to differ significantly from the ideal value for water19. In the open ocean, UV radiation can penetrate deep into the mixed layer of the water column. For example, in clear ocean waters of the Mediterranean Sea, UV radiation can cause phytoplankton mortality down to 26 m20. The difficulty in accurately predicting the penetration depth of UV-C in early seawater based on attenuation coefficients of modern seawater lies in the fact that today UV-C exposure is largely attenuated prior to reaching the Earth’s surface3. However, the absence of plant-derived humic substances and a protective ozone layer in the Archean may have allowed high-intensity UV radiation (including UV-C wavelengths) to reach greater depths in the ancient water column2. Cockell2 used a radiative transfer model that incorporated diffuse attenuation coefficients for the clearest modern ocean waters to predict that UV-B and UV-C radiation would have occurred at sufficient intensity to cause significant UV radiation-induced DNA damage throughout the mixed layer of the Archean ocean. Under these conditions it is likely that UV radiation would have been an even greater obstacle for early cyanobacteria than for their modern descendants.

Although a late origin for cyanobacteria has been proposed21, multiple lines of evidence suggest that planktonic populations of cyanobacteria evolved in and were able to persist through the Archean despite high fluxes of UV radiation22,23,24. An ancestral lineage and deep origin of planktonic cyanobacteria is inferred from the conservation of the GvpA and GvpC proteins that make up the gas vesicle walls designed to prevent them from sinking out of the euphotic zone15. Moreover, most mat-forming cyanobacteria have a free-floating stage in their life cycle which occurs in intertidal and near-shore areas of the coastal ocean and enables the colonization of new habitats25,26. So, although there is evidence for planktonic cyanobacteria in early marine environments from 2.7 Ga or earlier22,23,24, the means by which they overcame Archean UV radiation fluxes, and the scope of the effect of these fluxes on the biosphere remains uncertain.

Various dissolved and particulate iron species have been shown to be efficient absorbers of UV radiation, beginning with the pioneering study of Olson and Pierson27. The Archean oceans are generally agreed upon to have been dominated by anoxic-rich and iron-rich (ferruginous) conditions. Archean-dissolved marine Fe(II) concentrations are estimated to have been on the order of tens-to-hundreds of micromolar24,28, consistent with modern system Archean analogs29. In surface waters, a significant portion of this Fe(II) was oxidized to ferric oxyhydroxides, such as ferrihydrite, (Fe+3)2O3•0.5H2O, by anoxygenic photoferrotrophic bacteria30,31, which likely sedimented to the seafloor within a matter of days32. Iron isotope signatures in Archean banded iron formations (BIF) imply variable Fe(II) oxidation rates ranging from partial33 to near-complete34 within the ancient water column. Indeed, active communities of photoferrotrophic bacteria residing within modern, deep light-limited communities oxidize Fe(II) at a rate of up to 0.45 mol/m2/yr32, while Fe(II) oxidation rates of up to 50 mol/m2/yr have also been observed within the upper 15 m of the photic zone of a modern ferruginous basin34,35, enough to deposit the most voluminous BIF36. The ferric oxyhydroxides formed by these bacteria would have also provided protection from UV radiation when loosely attached to cell surfaces37.

Silica was another important component of Archean seawater, potentially reaching 2.2 mM38. Dissolved silica has a high affinity for ferric iron, and readily adsorbs onto the hydrous surfaces of iron oxides across a range of natural conditions39,40. Studies by Pierson et al.41 and Phoenix et al.44, using modern hot springs and experimental analogs, respectively, suggested that Fe(III)–silica gels and crusts overlying microbial mats could provide effective protection from UV-C radiation in Archean seawater. Here, building on this work, we explore the role of Fe(III)–silica precipitates in shaping the water column UV-C radiation profile and the resulting influence on cyanobacterial communities.

Through experimental analysis, we tested whether Fe(III)–Si precipitates forming in the Archean photic zone could have provided early planktonic cyanobacteria with an effective shield against UV-C radiation. It is impossible to sample the Precambrian biosphere directly, therefore, we rely on modern organisms as model systems. We explore these questions by growing the well-studied and fully sequenced marine cyanobacterium Synechococcus sp. PCC 7002 (hereafter Synechococcus) in Fe(III)- and Si-rich growth media simulating Archean seawater conditions24,28,38. We determined the effects on survival by exposing Synechococcus cultures to upper-end UV-C radiation fluxes (3 mW/cm2 at 254 nm)3, in experiments that were also used to understand UV radiation absorption by ancient seawater more generally. As per our experimental objective, UV-C radiation was chosen because, of the three classes of UV wavelength, it is the most harmful to life, and unlike today, it was an issue for inhabitants of Archean surface environments. DNA most readily absorbs at 260 nm and causes often lethal genetic damage (i.e., DNA strand breakage, mutagenic photoproducts such as cyclobutane pyrimidine dimers that inhibit transcription/replication of the chromosome)11. Low-pressure mercury lamps, such as the ones used in this study, are widely available and have a spectral peak at 254 nm—very close to DNA max absorbance, making this wavelength a reasonable choice to explore this problem. Furthermore, previous publications on protection from UV-C radiation by mat-forming cyanobacteria similarly used 254 nm, thus allowing comparison of attenuation effects in different modes of growth (i.e., planktonic vs. benthic)42. UV radiation fluxes were set to an order of magnitude higher than those predicted for the Archean (3 mW/cm2 compared with 0.4 mW/cm2)3 to provide a conservative estimate for the degree of efficiency with which these precipitates could protect cyanobacteria. Iron(III) (0.04–0.55 mM)24,28 and Si (0.6–2.0 mM)38 supplements were based on estimated Archean seawater concentrations, and we assumed a best case scenario of near-complete Fe(II) oxidation34.

Building from published geochemical constraints on Archean marine conditions and in-lab microbial growth and survival experiments, we were able to evaluate the extent of shielding from UV-C radiation that ferric iron precipitation in siliceous Archean seawater was likely to have provided for early planktonic cyanobacteria. We report that Fe(III)–Si precipitates suspended in the water column were able to absorb up to 70% of incident UV-C radiation while still transmitting the photosynthetically active radiation required for cyanobacterial growth. UV-C irradiated Synechococcus grown in iron–silica-rich growth media showed noticeably higher survival rates than irradiated cultures grown in un-supplemented media. However, we also observe that high mortality rates would have continued to limit cyanobacterial expansion, and suggest that these effects may have been felt throughout much of the Archean marine photic zone. These results imply that although Fe(III)–Si-rich precipitates would have played an important role in mitigating UV stress, this problem would not have been completely alleviated until atmospheric oxygen levels were sufficient to generate a protective ozone layer.


UV-C irradiation experiments

In this study, we test the ability of Fe(III) and Si to protect planktonic cyanobacteria from transitory exposure to high-intensity UV-C radiation. In the mixed layer of the modern photic zone, planktonic cells are at high risk of being transported to the ocean surface17, and we assume that this physical mechanism would also have existed in the Archean ocean. Synechococcus cultures exposed to UV-C radiation in Fe(III)- and Si-supplemented growth medium recover more rapidly from UV-C radiation stress than irradiated cultures in un-supplemented growth medium. In addition, growth rates increase steadily as initial Fe(III) and Si concentrations approach upper limits for Archean seawater (0.55 and 2.0 mM, respectively). Iron(III) or Si alone protect cells less efficiently from UV-C radiation than Fe(III) and Si combined. This is a crucial observation that implies that supplementation with both Fe(III) and Si is required for, and synergistically function as, a protective shield (Fig. 1a). This protective effect, though comparatively smaller, is also observed at Fe(III) concentrations of 40 μM. Lowermost Fe(II) concentrations for Archean seawater are predicted to range from 40 to 120 μM28, and assuming near-complete Fe(II) oxidation34, this may be a reasonable estimate for areas located distally from zones of iron-rich upwelling (Fig. 1b).

Fig. 1

Growth rates of UV-C irradiated Synechococcus cultures. Cultures were irradiated at an exposure of 500 J/m2 in Fe(III)- and Si-supplemented media relative to irradiated (dark circle: control UV) and un-irradiated (white circle: control) cultures in un-supplemented growth media. a Fe(III) concentrations representing environments proximal to a source of iron-rich upwelling. White diamond: low Fe(III)/Si, 0.15/0.6 mM; gray triangle: high Fe(III)/Si, 0.55/2.0 mM; white square: Si only, 2.0 mM; black square: Fe(III) only, 0.35 mM. b Fe(III) concentrations (0.04 mM) representing environments located distally from a source of iron-rich upwelling (i.e., background concentrations for Archean seawater25). Black triangle: background Fe(III)/Si 0.04/0.6 mM. Growth rates calculated on cultures grown in triplicate in two biological replicates, error bars represent standard deviation at 2σ uncertainty

Cell viability

The results reveal a positive correlation between initial Fe(III)–Si concentrations and cyanobacterial survival rates. However, cell viability assays show that UV-C irradiation at 500 J/m2 still dramatically reduce the population, with 97% mortality rate at the highest Fe(III)–Si concentrations. Survival increases from 0.13% viable cells in un-supplemented media to 2.76% at the highest Fe(III)–Si concentrations. In other words, the presence of Fe(III) and Si in the growth media facilitates the survival of only ~3% of the initial population following UV-C irradiation at 500 J/m2. This level is sufficient to seed a normal growth phase after 6 days (Fig. 2). Therefore, these results suggest that while Fe(III) and Si may have prevented high fluxes of UV radiation from sterilizing the early photic zone, UV radiation fluxes may still have had severe ecological impacts.

Fig. 2

Viability of UV-C irradiated Synechococcus cultures. Cultures grown at varying Fe(III) (0 mM, 0.15 mM, 0.35 mM, and 0.55 mM) and Si concentrations (white bar: 0.2 mM Si; light gray bar: 0.6 mM Si; dark gray bar: 2.0 mM Si) and irradiated with UV-C (254 nm) at 500 J/m2 were assessed by colony forming units (CFU) counts. Cultures grown at 0.55 mM Fe(III) and 0.2 mM Si died (horizontal line). Viability was calculated for cultures grown in triplicate in three biological replicates. Error bars represent standard deviation at 2σ uncertainty. Dashed line represents % survival in un-supplemented A+ growth medium

Light transmission by Fe(III)–Si precipitates

Unlike previous studies in which mineral coatings provide protection, our samples display fine-grained colloidal precipitates surrounding, but not directly attached to the cells, with sizes in the tens-of-nanometer range (Fig. 3). The additive nature of the UV-C radiation absorbance curves and their comparable slopes in cell-free, Fe(III)–Si and Fe(III)-only media solutions indicate that Fe(III) is the primary factor that controls the attenuation of UV-C radiation (Fig. 4a). Furthermore, attenuation assays on the same supplemented, cell-free growth medium concur with the growth rate analyses indicating that the Fe(III)–Si supplementation differentially and progressively attenuates UV-C radiation by 18% in Si-only media, 32% in Fe(III)-only media, and by 56% and 70% in the lowest and highest Fe(III)–Si end-member ratios, respectively (Fig. 4b). These filtration analyses indicate that nanoparticles (0.025–0.22 µm) and colloids (>0.22 µm) in Fe(III)–Si containing growth media absorb up to 40% and 32% of incoming UV-C radiation, respectively, and thus performed a significant role in the enhancement of survival of cyanobacteria in the presence of UV-C radiation.

Fig. 3

TEM imaging of Synechococcus cells and precipitates. a Transmission electron microscopy (TEM) image of nanoparticles surrounding (but not associated with) the cells in the presence of 0.35 mM Fe(III) and 2.0 mM Si. b TEM image showing the lack of biomineralization on Synechococcus. c Dark Fe(III)-rich precipitates and lighter salt nanoparticulates surrounding cells grown under conditions as shown in a

Fig. 4

UV-C attenuation in cell free, Fe(III)–Si-supplemented growth media. a Attenuation (% absorbance at 254 nm wavelengths) of UV-C radiation in unfiltered, cell-free growth medium supplemented with varying amounts of Si and Fe(III) (diamond: Fe(III) only; square: 0.6 mM Si; triangle: 2.0 mM Si). b UV-C attenuation in solutions that have been sequentially filtered to separate dissolved (<0.025 μm), nanoparticulate (0.025–0.22 μm), and colloidal (>0.22 μm) Fe(III)–Si fractions. Attenuation effects of the A+ medium have been subtracted. Error bars (if not shown than smaller than symbols) represent standard deviation at 2σ uncertainty

The photosynthetic production of O2 by cyanobacteria depends on chlorophyll, phycocyanin, and carotenoid pigments that selectively absorb PAR43. Modern, clear, natural waters attenuate wavelengths outside the PAR range more readily through absorption44 and scattering by both dissolved and particulate matter42. Although Fe(III) and Fe(III)–Si precipitates larger than 0.22 µm absorb some incoming PAR at these concentrations, >80% of PAR is still transmitted through the supplemented media at high end-member ratios (Fe(III)/Si: 0.55/2.0 mM), while 99% of PAR is transmitted at low end-member ratios (Fe(III)/Si: 0.04/0.6 mM) (Fig. 5).

Fig. 5

PAR transmission in cell-free, Fe(III)–Si-supplemented growth media. Transmission of photosynthetically active radiation (PAR: 400–700 nm; in %) through 0.04–0.55 mM Fe(III) (ad) and 0.6–2.0 mM Si (b, d) supplemented growth media. Upper curve—dissolved. Middle curve—nanoparticulate/dissolved. Bottom curve—colloidal/nanoparticulate/dissolved. Similar transmission of UV-C radiation in dissolved and nanoparticulate/dissolved fractions as show by overlap of the upper and middle curves


Our results demonstrate that although Fe(III)–Si precipitates would have moderated the impact of UV-C radiation stress on the survival of early cyanobacteria while not impeding cell growth, these UV-C radiation fluxes would have still limited cyanobacterial distribution within Archean marine photic environments. Similar to the presented results, biomineralized Fe(III)–Si crusts or gels encapsulating microbial mats are known to attenuate UV-C radiation while transmitting PAR in modern, benthic microbial communities41,42. As shown here and by others, Fe(III) on its own is known to be an efficient absorber of UV radiation especially at the shorter wavelengths41. The dominant form of the Fe(III) oxyhydroxide precipitates in our media is ferrihydrite as opposed to lepidocrocite, as ferrihydrite forms preferentially in solutions containing silica to iron ratios of 0.39 or higher (i.e., molar silica to iron ratios of experimental conditions here range from 1.9 to 9.3)45. The absence of solubility constants for polymeric Fe(III) and Fe(III)–Si complexes at circumneutral pH, as well as the amorphous nature of the precipitates, precludes accurate equilibrium speciation modeling of natural Fe(III)–Si-rich aqueous systems and X-ray fractionation for detailed particle characterization. Nonetheless, the formation of Fe(III)–Si precipitates has been characterized spectroscopically at lower pH46, and observations from the rock record strongly support the idea of a linked iron–silica cycle in the Archean47,48,49. Iron(III)–Si nanoparticles and colloids in Archean seawater would have formed as long as upwelling ferruginous waters and an oxidative mechanism persisted. Archean ferruginous waters likely occurred in both open ocean and coastal environments, as evidenced by thick successions of Neoarchean BIF interpreted to have been deposited in both deep and shallow marine settings50,51.

While we demonstrate that Fe(III) is the active UV radiation-absorbing ingredient in this system41, the major role of silica is to increase the stability of the colloidal and nanoparticulate ferrihydrite through the inhibition of Ostwald ripening52, thus delaying the formation of more stable Fe(III) (oxyhydr)oxides which would otherwise precipitate out of the water column. Silica will block dissolution sites or hinder the nucleation to more stable Fe(III) (oxyhydr)oxides at a pH > 3 by disrupting the corner-linkages between the iron-octahedra of the polymer, and by substituting itself into the second coordination-shell around the Fe(III) cation53. The effect of silica on colloidal stability has also been demonstrated experimentally in natural settings54. Longer colloidal settling times in a fluid occur as a function of increasing molar silica to iron ratio in solution55. Thus, in the absence of turbulence, published experimental work has established settling times of between 18 and 36 h in a saline solution for colloidal ferrihydrite formed under experimental molar silica to iron ratios comparable to the ones presented here56. These settling times, with flocculation being the dominant influence, would presumably increase in the presence of turbulence found in the mixed layer of the photic zone57. Multiple lines of evidence exist for pervasive co-precipitation of ferric iron and silica throughout the Archean water column47,48,49. Recent studies have suggested that the range of δ56Fe signatures found in Mesoarchean to Neoarchean aged BIF is best explained through isotopic fractionation during the co-precipitation of Fe(III) oxides and silica as well as through isotopic fractionation during the post-depositional, dissimilatory iron reduction of these precipitates48,49. In the modern Archean analog Lake Matano (Sulawesi, Indonesia), stable Fe(III) concentrations appear to be close to 100 nM—3 orders of magnitude lower than the aqueous Fe(II) concentration within the lake—while dissolved Si is only slightly lower than predicted for the Archean28. Therefore, further development of mechanistic models of Fe(III) removal from the water column at varying Fe(II) oxidation rates and Si concentrations are clearly required.

If we scale up our experimental results to explore the penetration depth of a given UV radiation flux based on the effects of Fe(III)–Si absorbance, we can consider the potential for UV-C radiation effects over water column relevant depths. Based on the Beer–Lambert law, there should be a linear relationship between absorbance and concentration in an ideal solution. However, our experimental results indicate that other factors, including particle aggregation and suspended particles in solution, cause a roughly lognormal relationship. By approximating this data with a log function, we consider the predicted absorbance based on the experimental data for a given path length (depth) and concentration of Fe(III) (Fig. 6). This modeling framework indicates that at Fe(III) concentrations similar to that of the Archean analog Lake Matano (100 nM)29, absorbance of UV-C radiation is ~80% at 60 m depth. At the UV-C flux used in this study, this level of radiation would be detrimental to the survival of cyanobacteria (Figs. 2 and 4). It is important to note that Archean UV-C fluxes are predicted to have been lower than our experimental levels so as to not overestimate the degree of efficiency with which the precipitates could protect cyanobacteria. Nevertheless, the flux of UV-A and UV-B radiation reaching the Earth’s surface in the Archean are also predicted to have been several times higher than today3. Therefore, this exercise provides a basic, conservative, scaled-up result suggesting that although Fe(II) oxidation in siliceous seawater would have mitigated UV radiation stress, it is still likely to have been a factor shaping ecosystems and potentially even the rates of primary productivity. This is consistent with the longstanding idea2 that pervasive UV-C radiation within the Archean photic zone would have been a significant obstacle for early cyanobacteria.

Fig. 6

Reaction transport model of predicted UV-C radiation absorbance with water column depth and Fe(III) concentration. Model parameters are based on experimental UV-C radiation (254 nm) attenuation data (% UV-C absorbed) in cell-free A+ media solutions, and assume iron redox dynamics similar to those in modern Archean analog site Lake Matano (Sulawesi, Indonesia)28

An effective protection mechanism against UV radiation would have been necessary not only for the survival, but more importantly, the propagation and expansion of early communities of cyanobacteria. The attenuation of UV-C radiation in natural water occurs as a function of dissolved and particulate matter suspended in the water column, as well as by the absorptive properties of the water itself. Today, elevated levels of largely plant-derived CDOM is an important component in the attenuation of UV radiation, and occurs primarily in coastal marine waters18. In the Archean, however, terrestrial organic input into the oceans was likely substantially less than the modern57.

Stress caused by UV-C radiation is also known to reduce metabolic O2 production through downregulation of genes encoding proteins involved in light harvesting and photosynthesis, photobleaching of photosynthetic pigments (e.g., phycocyanin, phycoerythrin), disintegration of phycobilisomes, and decreasing cellular chlorophyll and carotenoid contents11. While the base of the mixed layer may have presented cyanobacteria with a deep refuge from UV radiation2, it enhances the potential for at least seasonal light limitation on primary production over significant expanses of the oceans—a condition currently observed in the Southern Ocean58. Further, microorganisms living within the mixed layer are often carried to the surface where, even in modern environments, short periods of exposure to UV radiation can be inhibitory16. Deep chlorophyll maxima are typically below the bottom of the mixed layer, with maximum depths of ~100–150 m in parts of the western north Pacific and western Atlantic oceans where PAR irradiance is on the order of only 3–5% of that at the ocean’s surface2. Finally, lower overall solar luminosities in the Archean59 would have also increased the potential for light limitation60.

While oxygenic photosynthesis may have evolved sometime during the Mesoarchean22,23,24, our results suggest that environmental factors such as UV radiation stress (particularly from short wavelengths) may have contributed to limited primary production by early cyanobacteria. Despite the various mitigation strategies that have evolved in modern cyanobacteria7,8,9,10,11, UV-A and UV-B radiation fluxes in the upper photic zone of the modern oceans still present a considerable challenge (UV-C is largely attenuated by the ozone layer)16. Therefore, even if early cyanobacteria had modern UV radiation defense and repair mechanisms at their disposal, the higher fluxes of UV radiation reaching the Earth’s surface (especially UV-C) would have limited their productivity until a more efficient means of protection developed. An ozone layer would have been the most effective and permanent means of protection from UV-C radiation, but would not have fully developed until O2 levels reached ~1% PAL1,3, which likely did not occur until the mid-Proterozoic at the earliest as current estimates for mid-Proterozoic levels range from 0.1 to 10% PAL61,62.

Building on this framework, a major conclusion from this work is that despite the high Fe(III) and Si concentrations enabling their survival, UV-C irradiation still could have induced high rates of mortality for planktonic communities of cyanobacteria in the upper reaches of the water column. Extrapolating beyond Earth, these limiting effects have implications for the potential of light-limited exoplanetary biospheres5,6. While Fe(III)–Si particles and colloids contributed to the mitigation of limited ozone concentrations, the presence of these chemical species would not have alleviated the UV radiation problem completely, as has been suggested for benthic communities41,42. Thus, future Archean global biogeochemical models should work to directly integrate the effects of UV irradiation on the delineation and organismal composition of the biosphere.



The marine planktonic cyanobacterium Synechococcus sp. PCC 7002 (previously known as Agmenellum quadruplicatum)63 is a unicellular, euryhaline, marine cyanobacterium. It was chosen as the model organism due to its adaptation to higher light conditions and dissolved iron levels compared with other strains of Synechococcus and Prochlorococcus64,65. The laboratory wild-type strain was originally obtained from Professor Donald Bryant at Pennsylvania State University.


Axenic cultures were grown in A+ medium66: 0.31 M NaCl; 8 mM KCl; 12 mM NaNO3; 20 mM MgSO4•7H2O; 0.37 mM KH2PO4; 2.4 mM CaCl2; 0.08 mM Na2EDTA•2H2O; 0.014 mM FeCl3•6H2O; 8.25 mM Tris HCl (pH 8.2); P-1 metals (0.55 mM H3BO4; 22 µM MnCl2•4H2O; 2.3 µM ZnCl2; 0.22 µM MoO3 (85%); 0.012 µM CuSO4•5H2O; 0.051 µM CoCl2•6H2O); and 59 nM vitamin B12 prepared in 18.2 MΩ cm MilliQ water. See Supplementary Note 1 for a discussion on the effects of EDTA on Fe(III) and Si reactivity in A+ growth medium (Supplementary Fig. 1). Axenic stock populations were maintained on 1.5% (w/v) A+ agar in Petri dishes at 30 °C under constant illumination (~50 µmol photons/m2/s). Cultures for inoculating experiments were prepared from agar-based cultures by suspension of cyanobacteria into 50 mL of media in 250 mL borosilicate glass Erlenmeyer flasks with gas-permeable foam stoppers (Canlab Dispo Plugs). In order to obtain sufficient biomass for Fe(III) and Si growth experiments from a single culture, 300 mL cultures were grown in 1 L borosilicate glass Erlenmeyer flasks with gas-permeable foam stoppers and bubbled with sterile air to enhance CO2 supply. The 14% v/v inoculum used to establish these 300 mL cultures was derived from a single 50 mL liquid culture. The 300-mL culture was then used to inoculate 50 mL experimental cultures in A+ medium supplemented with concentrations of Si as Na2SiO3 (to final Si concentrations of 0.2 mM, 0.6 mM, and 2.0 mM) and Fe(III) as FeCl3•6H2O in the A+ media (to final Fe(III) concentrations of 0.04 mM, 0.15 mM, 0.35 mM, and 0.55 mM). Control experiments (un-irradiated cultures grown in A+ medium with no added iron and silica) were also included, as well as cultures grown in Fe(III)-only supplemented A+ medium and Si-only supplemented A+ medium to ascertain the effects of these compounds individually on growth rate. Cultures were grown in triplicate, and experiments repeated in two independent biological replicates. Stock cultures for inoculating experiments were harvested when optical density measurements at a wavelength of 750 nm (OD750) indicated that they had reached mid-exponential growth phase (~4 × 106 cells/mL).

The oxic conditions used for these experiments do not preclude the main premise of this study, to examine whether Fe(III)–Si precipitates suspended in the water column could protect planktonic cyanobacteria from UV-C radiation. As evidenced in the BIF record, Fe(III) oxides were ubiquitous in the Archean water column. Once cyanobacteria had evolved, the microenvironment proximal to cells of cyanobacteria would have contained free O222,23,24. And although the mechanisms of Archean Fe(II) oxidation prior to the evolution of oxygenic photosynthesis are still debated, it has been argued that photoferrotrophs metabolically oxidizing Fe(II) in the ancient photic zone were the most plausible producers of Fe(III), although Fe(II) photo-oxidation and reaction with hydrogen peroxide, albeit less productive processes, were other potential mechanisms30,31.

UV irradiation

To ascertain the effects of silica and ferric iron during the UV irradiation of live cells, cultures were irradiated in a Stratalinker UV Crosslinker 1800 containing 5 × 254 nm (8 W) bulbs collectively emitting radiation at 3 W/cm2 (Supplementary Fig. 2). Experimental cultures were harvested at mid-exponential phase (OD750 indicating ~4 × 106 cells/mL), where 10 mL were transferred into sterile plastic Petri dishes (no lid) using a sterile glass pipette so that the entire surface was covered by a thin layer of liquid (Supplementary Fig. 3). Cultures were irradiated at 500 J/m2 (i.e., 3 mW/cm2 for 16.7 s) followed by a 6-h dark incubation. The selected dose of UV-C radiation was based on maximal depression of cell viability in un-supplemented cultures (Supplementary Fig. 4). Samples were then grown at 30 °C under full spectrum fluorescent light (Philips F48T12/CW/HO 60 W) where wavelengths < 520 nm were filtered out (Roscolux Supergel filter plastic #15) to prevent photoreactivation of nucleic acids damaged by UV radiation. These measures were taken to ensure that the data represented growth and viability as a direct result of UV radiation damage. Incubation periods varied from 7 to 19 days to ascertain patterns of immediate recovery as well as long-term viability and growth.

Determination of cell viability post-UV irradiation

Total chlorophyll a concentration was used as proxy for growth rate67, and cultures were sampled in duplicate every day or every second day for chlorophyll a and OD750 measurements. As a measure of cell viability in irradiated samples, the ratio of live to dead cells was used and determined by counting the number of colony forming units (CFU). Appropriately diluted aliquots (100 µL) of irradiated, dark incubated samples were plated on A+ agar and subsequently incubated under optimal light conditions (with filtered wavelengths < 520 nm to prevent photoreactivation, as described above) for 10 days. When grown at a temperature of 30 °C in A+ medium, a cell suspension with OD750 = 1 typically contained 6.3 ± 0.4 × 108 cells per mL (n = 3) as determined by microscopic counts, and a count of 2.1 ± 0.6 × 108 cfu per mL (n = 3). Each treatment was done in triplicate, and repeated in three biological replicates.

Light transmission and particle size characterization

The attenuation of UV-C radiation (254 nm) and photosynthetically active radiation (PAR: 400–700 nm) by Fe(III)- and Si-supplemented growth media was determined in triplicate on a Pharmacia Ultrospec 3000 spectrophotometer using quartz (for UV-C) and polystyrene (for PAR) cuvettes with 1 cm path lengths. Attenuation by various Fe(III)–Si size fractions were also determined by filtering media solutions twice using cellulose acetate Millipore filters, firstly to 0.22 µm, whereupon the attenuation of UV-C radiation at 254 nm and PAR transmission was measured. The resulting filtrate was subsequently filtered to 0.025 µm and measurement attenuation of UV-C radiation at 254 nm and PAR transmission repeated. Results for the various size fractions were determined by normalizing results to those of unfiltered, un-supplemented solutions in order to take into account the effects of total dissolved solids in the saline medium.

Transmission electron microscopy

For transmission electron microscopy (TEM) imaging of the cells, Synechococcus cultures grown in Fe(III)- and Si-supplemented A+ media were fixed in a solution of 2.5% gluteraldehyde + 2% Paraformaldehyde, dehydrated through an ascending ethanol series (50–100%), stained with 1% osmium tetroxide, embedded in Spurr low viscosity resin, thin sectioned (80–100 nm) using a Reichert-Jung Ultracut E microtome, and sections stained with 2% uranyl acetate. For images of the Fe(III)–Si precipitates, a drop of cell-free media was spread onto a cellulose film supported by a copper grid. TEM images were obtained using a Philips/FEI Morgagni 268 TEM operating at 80 kV equipped with a Gatan Orius Digital Camera using Gatan Digital Micrograph version 1.81.78 imaging software.

UV-C penetration estimates

Our estimate for the penetration depth of UV-C radiation was based directly on experimental results, and therefore reflects an estimate for monochromatic penetration of UV radiation at 254 nm. A log function was fit to the measured absorbance of UV-C radiation 0.6 mM Si resulting from changing concentrations of Fe(III) (Fig. 4). Because the absorbance of UV-C radiation was measured over a 1 cm path length, we considered the moles of Fe(III) present over a given path length, and compared that to percentage absorbance predicted by our experimentally-derived log function for the same number of moles within 1 cm3 volume.

Data availability

The data sets generated during and/or analyzed during the current study are available from the corresponding authors on reasonable request.


  1. 1.

    Kasting, J. F. Theoretical constraints on oxygen and carbon dioxide concentrations in the Precambrian atmosphere. Precambrian Res. 34, 205–229 (1987).

    Article  PubMed  ADS  CAS  Google Scholar 

  2. 2.

    Cockell, C. S. Ultraviolet radiation and the photobiology of Earth’s early oceans. Orig. Life Evol. Biosph. 30, 467–499 (2000).

    Article  PubMed  ADS  CAS  Google Scholar 

  3. 3.

    Segura, A. et al. Ozone concentrations and ultraviolet fluxes on Earth-like planets around other stars. Astrobiology 3, 689–708 (2003).

    Article  PubMed  ADS  CAS  Google Scholar 

  4. 4.

    Castenholz, R. W. & Garcia-Pichel, F. in Ecology of Cyanobacteria II: Their Diversity in Space and Time (ed. Whitton, B. A.) 481–499 (Springer Netherlands, Dordrecht, 2000).

  5. 5.

    O’Malley-James, J. T. & Kaltenegger, L. UV surface habitability of the TRAPPIST-1 system. Mon. Not. R. Astron 469, L26–L30 (2017).

    Article  ADS  Google Scholar 

  6. 6.

    Anglada-Escudé, G. et al. A terrestrial planet candidate in a temperate orbit around Proxima Centauri. Nature 536, 437–440 (2016).

    Article  PubMed  ADS  CAS  Google Scholar 

  7. 7.

    O’Brian, P. A. & Houghton, J. A. Photoreactivation and excision repair of UV induced pyrimidine dimers in the unicellular cyanobacterium Gloeocapsa alpicola (Synechocystis PCC 6308). Photochem. Photobiol. 35, 359–364 (1982).

    Google Scholar 

  8. 8.

    Owttrim, G. W. & Coleman, J. R. Regulation of expression and nucleotide sequence of the Anabaena variabilis recA gene. J. Bacteriol. 171, 5713–5719 (1989).

    Article  PubMed  PubMed Central  CAS  Google Scholar 

  9. 9.

    Mittler, R. & Tel-Or, E. Oxidative stress responses in the unicellular cyanobacterium Synechococcus PCC 7942. Free Radic. Res. Commun. 12, 845–850 (1991).

    Article  PubMed  Google Scholar 

  10. 10.

    Ehling-Shultz, M., Bilger, W. & Scherer, S. UV-B-induced synthesis of photoprotective pigments and extracellular polysaccharides in the terrestrial cyanobacterium Nostoc commune. J. Bact. 179, 1940–1945 (1997).

    Article  Google Scholar 

  11. 11.

    Singh, S. P., Hader, D.-P. & Sinha, R. P. Cyanobacteria and ultraviolet radiation (UV) stress: mitigation strategies. Ageing Res. Rev. 9, 79–90 (2010).

    Article  PubMed  CAS  Google Scholar 

  12. 12.

    Garcia‐Pichel, F. A. A model for internal self‐shading in planktonic organisms and its implications for the usefulness of ultraviolet sunscreens. Limnol. Oceanogr. 39, 1704–1717 (1994).

    Article  ADS  Google Scholar 

  13. 13.

    Phoenix, V. R., Bennett, P. C., Engel, A. S., Tyler, S. W. & Ferris, F. G. Chilean high-altitude hot-spring sinters: a model system for UV screening mechanisms by early Precambrian cyanobacteria. Geobiology 4, 15–28 (2006).

    Article  CAS  Google Scholar 

  14. 14.

    Garcia-Pichel, F., Mechling, M. & Castenholz, R. W. Diel migrations of microorganisms within a benthic, hypersaline mat community. Appl. Environm. Microbiol. 60, 1500–1511 (1994).

    CAS  Google Scholar 

  15. 15.

    Griffiths, A. E., Walsby, A. E. & Hayes, P. K. The homologies of gas vesicle proteins. Microbiology 138, 1243–1250 (1992).

    CAS  Google Scholar 

  16. 16.

    Neale, P. J., Davis, R. F. & Cullen, J. J. Interactive effects of ozone depletion and vertical mixing on the photosynthesis of Antarctic phytoplankton. Nature 392, 585–589 (1998).

    Article  ADS  CAS  Google Scholar 

  17. 17.

    Cullen, J. J. & Neale, P. J. Ultraviolet radiation, ozone depletion, and marine photosynthesis. Photo. Res. 39, 303–320 (1994).

    Article  CAS  Google Scholar 

  18. 18.

    Bricaud, A., Morel, A. & Louis, P. Absorption by dissolved organic matter of the sea (yellow substance) in the UV and visible domains. Limnol. Oceanogr. 26, 43–53 (1981).

    Article  ADS  CAS  Google Scholar 

  19. 19.

    Kirk, J. T. Light and Photosynthesis in Aquatic Ecosystems 2nd edn (Cambridge University Press, Cambridge, 1994).

  20. 20.

    Llabrés, M. et al. Synechococcus and Prochlorococcus cell death induced by UV radiation and the penetration of lethal UVR in the Mediterranean Sea. Mar. Ecol. Prog. Ser. 399, 27–37 (2010).

    Article  ADS  CAS  Google Scholar 

  21. 21.

    Kirschvink, J. L. & Kopp, R. E. Palaeoproterozoic ice houses and the evolution of oxygen-mediating enzymes: the case for a late origin of photosystem II. Philos. Trans. R Soc. B 363, 2755–2765 (2008).

    Article  CAS  Google Scholar 

  22. 22.

    Crowe, S. A. et al. Atmospheric oxygenation three billion years ago. Nature 50, 535–538 (2013).

    Article  ADS  CAS  Google Scholar 

  23. 23.

    Planavsky, N. J. et al. Evidence for oxygenic photosynthesis half a billion years before the great oxidation event. Nat. Geosci. 7, 283–286 (2014).

    Article  ADS  CAS  Google Scholar 

  24. 24.

    Czaja, A. D. et al. Evidence for free oxygen in the Neoarchean ocean based on coupled iron–molybdenum isotope fractionation. Geochim. Cosmochim. Acta 86, 118–137 (2012).

    Article  ADS  CAS  Google Scholar 

  25. 25.

    Stoodley, P., Sauer, K., Davies, D. G. & Costerton, J. W. Biofilms as complex differentiated communities. Ann. Rev. Microbiol. 56, 187–209 (2002).

    Article  CAS  Google Scholar 

  26. 26.

    Nagar, E. & Schwarz, R. To be or not to be planktonic? Self-inhibition of biofilm development. Env. Microbiol. 17, 1477–1486 (2015).

    Article  CAS  Google Scholar 

  27. 27.

    Olson, J. M. & Pierson, B. K. Photosynthesis 3.5 thousand million years ago. Photo. Res. 9, 251–259 (1986).

    Article  CAS  Google Scholar 

  28. 28.

    Canfield, D. E. The early history of atmospheric oxygen: homage to Robert M. Garrels. Annu. Rev. Earth Planet. Sci. 33, 1–36 (2005).

    Article  ADS  CAS  Google Scholar 

  29. 29.

    Crowe, S. A. et al. The biogeochemistry of tropical lakes: a case study from Lake Matano, Indonesia. Limnol. Oceanogr. 53, 319–331 (2008).

    Article  ADS  CAS  Google Scholar 

  30. 30.

    Kappler, A. et al. Deposition of banded iron formations by anoxygenic phototrophic Fe (II)-oxidizing bacteria. Geology 33, 865–868 (2005).

    Article  ADS  CAS  Google Scholar 

  31. 31.

    Konhauser, K. O. et al. Could bacteria have formed the Precambrian banded iron formations? Geology 30, 1079–1082 (2002).

    Article  ADS  CAS  Google Scholar 

  32. 32.

    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).

    Article  CAS  Google Scholar 

  33. 33.

    Dauphas, N., Cates, N. L., Mojzsis, S. J. & Busigny, V. Identification of chemical sedimentary protoliths using iron isotopes in the > 3750 Ma Nuvvuagittuq supracrustal belt, Canada. Earth Planet. Sci. Lett. 254, 358–376 (2007).

    Article  ADS  CAS  Google Scholar 

  34. 34.

    Johnson, C. M. et al. Iron isotopes constrain biologic and abiologic processes in banded iron formation genesis. Geochim. Cosmochim. Acta 72, 151–169 (2008).

    Article  ADS  CAS  Google Scholar 

  35. 35.

    Llirós, M. et al. Pelagic photoferrotrophy and iron cycling in a modern ferruginous basin. Sci. Rep. 5, 13803 (2015).

  36. 36.

    Konhauser, K. O. et al. Phytoplankton contributions to the trace-element composition of Precambrian banded iron formations. Geol. Soc. Am. Bull. 130, 941–951 (2017).

    Article  Google Scholar 

  37. 37.

    Gauger, T., Konhauser, K. & Kappler, A. Protection of phototrophic iron (II)-oxidizing bacteria from UV irradiation by biogenic iron (III) minerals: implications for early Archean banded iron formation. Geology 43, 1067–1070 (2015).

    CAS  Google Scholar 

  38. 38.

    Maliva, R. G., Knoll, A. H. & Simonson, B. M. Secular change in the Precambrian silica cycle: insight from chert petrology. Geol. Soc. Am. Bull. 117, 835–845 (2005).

    Article  ADS  Google Scholar 

  39. 39.

    Davis, C. C., Chen, H. W. & Edwards, M. Modeling silica sorption to iron hydroxide. Environ. Sci. Technol. 36, 582–587 (2002).

    Article  PubMed  ADS  CAS  Google Scholar 

  40. 40.

    Konhauser, K. O. et al. Decoupling photochemical Fe (II) oxidation from shallow-water BIF deposition. Earth Planet. Sci. Let. 258, 87–100 (2002).

    Article  ADS  CAS  Google Scholar 

  41. 41.

    Pierson, B. K., Mitchell, H. K. & Ruff-Roberts, A. L. Chloroflexus aurantiacus and ultraviolet radiation: implications for Archean shallow-water stromatolites. Orig. Life Evol. Biosph. 23, 243–260 (1993).

    Article  ADS  Google Scholar 

  42. 42.

    Phoenix, V. R., Konhauser, K. O., Adams, D. G. & Bottrell, S. H. Role of biomineralization as an ultraviolet shield: implications for Archean life. Geology 29, 823–826 (2001).

    Article  ADS  CAS  Google Scholar 

  43. 43.

    Kishino, M., Takahashi, M., Okami, N. & Ichimura, S. Estimation of the spectral absorption coefficients of phytoplankton in the sea. Bull. Mar. Sci. 37, 634–642 (1985).

    Google Scholar 

  44. 44.

    Smith, R. C. & Baker, K. S. Optical properties of the clearest natural waters. Appl. Opt. 20, 177–184 (1981).

    Article  PubMed  ADS  CAS  Google Scholar 

  45. 45.

    Schwertmann, U., Carlson, L. & Fechter, H. Iron oxide formation in artificial ground waters. Aquat. Sci. 46, 185–191 (1984).

    Article  Google Scholar 

  46. 46.

    Pokrovski, G. S., Schott, J., Farges, F. & Hazemann, J.-L. Iron(III)-silica interactions in aqueous solutions: insight from x-ray absorption fine structure spectroscopy. Geochim. Cosmochim. Acta 19, 3559–3573 (2003).

    Article  ADS  CAS  Google Scholar 

  47. 47.

    Fischer, W. W. & Knoll, A. H. An iron shuttle for deep water silica in Late Archean and early Paleoproterozoic iron formation. Geol. Soc. Am. Bull. 121, 222–235 (2009).

    Google Scholar 

  48. 48.

    Percak-Dennett, L., Roden, E. E., Beard, B. L. & Johnson, C. M. Iron isotope fractionation during dissimilatory iron reduction under simulated Archean conditions. Geobiology 9, 205–220 (2011).

    Article  PubMed  CAS  Google Scholar 

  49. 49.

    Wu, L., Percak-Dennett, E. M., Beard, B. L., Roden, E. E. & Johnson, C. M. Stable iron isotope fractionation between aqueous Fe(II) and model Archean ocean Fe–Si co precipitates and implications for iron isotope variations in the ancient rock record. Geochim. Cosmochim. Acta 84, 14–28 (2012).

    Article  ADS  CAS  Google Scholar 

  50. 50.

    Fralick, P. & Pufahl, P. K. Iron formation in Neoarchean deltaic successions and the microbially mediated deposition of transgressive systems tracts. J. Sed. Res. 76, 1057–1066 (2010).

    Article  CAS  Google Scholar 

  51. 51.

    Konhauser, K. O. et al. Iron formations: a global record of Neoarchaean to Palaeoproterozoic environmental history. Earth Sci. Rev. 172, 140–177 (2017).

    Article  CAS  Google Scholar 

  52. 52.

    Cornell, R. M. & Schwertmann, U. The Iron Oxides: Structure, Properties, Reactions, Occurrences And Uses 2nd ed (John Wiley & Sons, Hoboken, NJ, 2003).

  53. 53.

    Cismasu, A. C., Michel, F. M., Tcaciuc, A. P. & Brown, G. E. Jr. Properties of impurity-bearing ferrihydrite III. Effects of Si on the structure of 2-line ferrihydrite. Geochim. Cosmochim. Acta 133, 168–185 (2014).

    Article  ADS  CAS  Google Scholar 

  54. 54.

    Jones, A. M. et al. The effect of silica and natural organic matter on the Fe (II)-catalysed transformation and reactivity of Fe (III) minerals. Geochim. Cosmochim. Acta 73, 4409–4422 (2009).

    Article  ADS  CAS  Google Scholar 

  55. 55.

    Mayer, T. D. & Jarrell, W. M. Formation and stability of iron (II) oxidation products under natural concentrations of dissolved silica. Water Res. 30, 1208–1214 (1996).

    Article  CAS  Google Scholar 

  56. 56.

    McCave, I. N. Erosion, transport and deposition of fine-grained marine sediments. Geol. Soc. Lond. Spec. Publ. 15, 35–69 (1984).

    Article  ADS  Google Scholar 

  57. 57.

    Kenrick, P. & Crane, P. R. The origin and early evolution of plants on land. Nature 389, 33–39 (1997).

    Article  ADS  CAS  Google Scholar 

  58. 58.

    Garcia-Pichel, F. Solar ultraviolet and the evolutionary history of cyanobacteria. Orig. Life Evol. Biosph. 28, 321–347 (1998).

    Article  PubMed  ADS  CAS  Google Scholar 

  59. 59.

    Mitchell, B. G., Brody, E. A., Holm‐Hansen, O., McClain, C. & Bishop, J. Light limitation of phytoplankton biomass and macronutrient utilization in the Southern Ocean. Limnol. Oceanogr. 36, 1662–1677 (1991).

    Article  ADS  Google Scholar 

  60. 60.

    Sagan, C. & Mullen, G. Earth and Mars: evolution of atmospheres and surface temperatures. Science 177, 52–56 (1972).

    Article  PubMed  ADS  CAS  Google Scholar 

  61. 61.

    Cole, D. B. et al. A shale-hosted Cr isotope record of low atmospheric oxygen during the Proterozoic. Geology 44, 555–558 (2016).

    Article  ADS  CAS  Google Scholar 

  62. 62.

    Daines, S. J., Mills, B. J. & Lenton, T. M. Atmospheric oxygen regulation at low Proterozoic levels by incomplete oxidative weathering of sedimentary organic carbon. Nat. Commun. 8, 14379 (2017).

  63. 63.

    Ludwig, M. & Bryant, D. A. Synechococcus sp. PCC 7002 transcriptiome: acclimation to temperature, salinity, oxidative stress and mixotrophic growth conditions. Front. Microbiol. 3, 1–14 (2012).

    Google Scholar 

  64. 64.

    Morris, J. J., Johnson, Z. I., Szul, M. J., Keller, M. & Zinser, E. R. Cyanobacterium Prochloroccocus on hydrogen peroxide scavenging microbes for growth at the ocean’s surface. PLoS ONE 6, e16805 (2011).

    Article  PubMed  PubMed Central  ADS  CAS  Google Scholar 

  65. 65.

    Rusch, D., Martiny, A. C., Dupont, C. L., Halpern, A. L. & Venter, J. C. Characterization of Prochloroccocus clades from iron-depleted oceanic regions. Proc. Natl Acad. Sci. USA 107, 16184–16189 (2010).

    Article  PubMed  ADS  Google Scholar 

  66. 66.

    Stevens, S. E. & Porter, R. D. Transformation in Agmenellum quadruplicatum. Proc. Natl Acad. Sci. USA 77, 6052–6056 (1980).

    Article  PubMed  ADS  CAS  Google Scholar 

  67. 67.

    Porra, R. J., Thompson, W. A. & Kriedemann, P. E. Determination of accurate extinction coefficients and simultaneous equations for assaying chlorophyll a and b extraction with four different solvents: verification of the concentration of chlorophyll standards by atomic absorption spectroscopy. Biochim. Biophys. Acta 975, 384–394 (1989).

    Article  CAS  Google Scholar 

Download references


We acknowledge NSERC Discovery Grants to K.O.K. and G.W.O., an NSERC PGSD to A.M.M., and funding from the NASA Alternative Earths Astrobiology Institute to N.J.P. We also thank Arlene Oatway for her assistance with TEM imaging (Advanced Microscopy Facility, University of Alberta).

Author information




Experimental design: A.M.M., G.W.O., and K.O.K. Experiments: A.M.M. with major contributions from N.J.P. and D.S.W. Data analysis: A.M.M., G.W.O., K.O.K., D.S.W., N.J.P., D.B.C., and A.K. Writing of the manuscript: A.M.M. with major contributions from K.O.K., G.W.O., D.S.W., D.B.C., and A.K.

Corresponding authors

Correspondence to Aleksandra M. Mloszewska or Kurt. O Konhauser.

Ethics declarations

Competing interests

The authors declare no competing interests.

Additional information

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

Electronic supplementary material

Rights and permissions

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

Reprints and Permissions

About this article

Verify currency and authenticity via CrossMark

Cite this article

Mloszewska, A.M., Cole, D.B., Planavsky, N.J. et al. UV radiation limited the expansion of cyanobacteria in early marine photic environments. Nat Commun 9, 3088 (2018).

Download citation

Further reading


By submitting a comment you agree to abide by our Terms and Community Guidelines. If you find something abusive or that does not comply with our terms or guidelines please flag it as inappropriate.


Quick links

Nature Briefing

Sign up for the Nature Briefing newsletter — what matters in science, free to your inbox daily.

Get the most important science stories of the day, free in your inbox. Sign up for Nature Briefing