The Eridania region in the southern highlands of Mars once contained a vast inland sea with a volume of water greater than that of all other Martian lakes combined. Here we show that the most ancient materials within Eridania are thick (>400 m), massive (not bedded), mottled deposits containing saponite, talc-saponite, Fe-rich mica (for example, glauconite-nontronite), Fe- and Mg-serpentine, Mg-Fe-Ca-carbonate and probable Fe-sulphide that likely formed in a deep water (500–1,500 m) hydrothermal setting. The Eridania basin occurs within some of the most ancient terrain on Mars where striking evidence for remnant magnetism might suggest an early phase of crustal spreading. The relatively well-preserved seafloor hydrothermal deposits in Eridania are contemporaneous with the earliest evidence for life on Earth in potentially similar environments 3.8 billion years ago, and might provide an invaluable window into the environmental conditions of early Earth.
The oldest supracrustal rocks on Earth are early Eoarchean seafloor deposits (≥3.7 Ga)1. The presence of isotopically light carbon2 within biogenic morphologies in these rocks indicates that life may have flourished on the early Earth in hydrothermal seafloor environments3. Yet progress in further understanding the actual origin of life or prebiotic chemistry from these rocks, or those of similar age, is severely challenged by the fact that they have experienced multiple generations of metamorphism, metasomatism and deformation4. The search for life’s origins through empirical geologic evidence might require exploration beyond Earth, where younger geological activity has not overwritten critically important chemical and textural records. This journey could lead to Mars where ancient sedimentary, volcanic and hydrothermal deposits contemporaneous with the origin of life on Earth have escaped deep burial and metamorphism.
The Eridania region, located at the boundary of Terra Cimmeria and Terra Sirenum (Fig. 1), includes exposures of some of the most ancient terrain on Mars5. This area exhibits the strongest evidence for remnant magnetism on Mars and could be a site of ancient crustal spreading6 (Fig. 1a). Geophysical models suggest that the area had a high thermal gradient in the Noachian7, consistent with regional magmatism. The presence of a high-potassium anomaly8 could be an indication of a deep mantle source for ancient volcanism in the area or widespread alteration of the crust9,10. Regardless of whether the remnant magnetism is truly indicative of early plate tectonics, the fact that the magnetic signature is observed is an indication that the near surface materials formed when the magnetic field of Mars was strong, and have not been buried as has occurred in other areas5. Therefore, the geology observed here provides insights into geological processes that operated in the earliest observable epoch of Martian history11.
In addition to containing come of the most ancient crust on Mars, the Eridania region is important because it contains a large basin that was once filled with water. In this study, we examined the geology and mineralogy of the most ancient deposits within this basin. Using infrared spectroscopy and high-resolution imaging, we show that the Eridania basin contains a complex suite of alteration minerals that likely formed in a hydrothermal seafloor volcanic-sedimentary setting.
Geomorphic evidence for an ancient sea in Eridania basin
Eridania basin is composed of a series of connected, smaller, quasi-circular basins (Fig. 1), which potentially originated as very ancient impacts that were resurfaced by volcanism and erosion early in Mars' history12,13. The extent of the Eridania basin was previously defined as the 1,100 m elevation contour around these sub-basins13 (Fig. 1). Irwin et al.13 deduced that the Eridania basin was once filled to this level because it is at this elevation that the 3-km-wide Ma’adim Vallis outflow channel originates (Fig. 1c)13. This morphology, with a complete lack of upstream tributaries, suggests that the channel formed at full width, although a spillway at the edge of the Eridania basin at ∼1,100 m elevation, a strong indication that the basin was filled with water at the Noachian/Hesperian boundary13.
Irwin et al.13 recognized the unusual hypsometry of the Eridania basins, noting that they have unusual concave topographic profiles. We similarly compare the topographic data of Eridania basins to data of basins elsewhere on Mars (Supplementary Fig. 1). Most similar sized basins elsewhere on Mars exhibit clear ‘U-shaped’ topographic profiles which arise from colluvial, fluvial and volcanic resurfacing of the basins in a subaerial setting. The concave structure of the Eridania basins is an indication that, during the only intense period of erosive activity in mars history, these basins were protected beneath water or ice-covered water.
Previous researchers noted that Noachian valley networks also terminate at an elevation of ∼700–1,100 m (refs 13, 14), suggesting the existence of an ancient base level. If a water level existed between 700 and 1,100 m elevation, the basin topography implies that the parts of the lake would have been 1–1.5 km deep. The approximate size of such a body of water would have been ∼1.1 × 106 km2, ∼3 × larger than the largest landlocked lake or sea on Earth (Caspian Sea) (Fig. 2). In fact, even a conservative estimate of the volume of the Eridania sea exceeds the total volume of all other lakes on Mars combined (Fig. 2)15. Here we synthesize previous work and provide new analyses of the mineralogy, geology, and context of the most ancient deposits in Eridania basin (Fig. 1c), which we argue formed in a deep-water hydrothermal setting.
Multiple types of colles and chaos units in Eridania basin
Unique deposits found only at the centre (deepest part) of each basin (Fig. 1c) consist of fractured and dismembered blocks ∼0.1–10 km diameter (Fig. 3). While these deep basin units are in some cases formally named ‘chaos’ and in other cases, ‘colles16,’ there are some clear and important geological differences among the deposits that are not reflected in the naming convention and often confused in previous work (Fig. 3). Most importantly, the fractured blocks in the western and central parts of Eridania, as we argue in this paper, represent ancient, deep basin subaqueous units and those in the eastern parts of the basin are younger, eroded volcanics deposited subaerially.
Ariadnes Colles and Atlantis Chaos contain the best examples of deep basin deposits (Fig. 3a–c) that formed in deep water16. There, massive blocks of bedrock (lacking observable bedding) reach up to 400 m elevation above the surrounding dark-toned plains (Fig. 4). The deep basin unit was eroded and dismembered into buttes and mesas, subsequently embayed and blanketed by volcanic materials in the Hesperian, resulting in a kīpuka-like landscape (Fig. 4).
By contrast, block-forming units observed to the east in Gorgonum are completely different in terms of texture, bedding17, colour and mineralogy (Fig. 3d–f ). These units are characterized by the presence of smaller blocks composed of a mixture of boulders and friable materials. Texturally, they are smooth and hummocky, and they have been widely eroded to form gullies in many cases18, which is rare in the deep basin deposits to the west except where mantling volcanic deposits occur. The younger chaos units never show mottled colour patterns and do not contain evidence for fractures and veins. These are eroded blocks within the younger, superposed volcanic material (likely both ash and lava).
The block-forming basin unit in Gorgonum is substantially younger than the deep basin units in Ariadnes or Atlantis. Crater counting was performed within the deep basin deposits to estimate minimum ages for those deposits. We counted craters with diameters ≥500 m throughout the deep basin deposits using Mars Context Imager (CTX) data as the base. The key result is that that deposits in Ariadnes and Atlantis basins are much older than basin deposits in eastern basins, especially Gorgonum. Assuming a crater producton function from Ivanov (2001) and absolute chronology based on Hartmann and Neukum19,20, we estimate that minimum exposure age for the Ariadnes deposits at 3.77 Ga and the Gorgonum deposits at 3.47 Ga (Supplementary Fig. 2). These ages are consistent with previous results, which suggest that the Eridania basin-forming impacts occurred >4 Ga, the sea existed in the Late Noachian and was resurfaced by subaerial volcanism in the Late Hesperian5,12,13,16. A key new conclusion is that, while all of the Eridania sub-basins likely contained deep water environments, the deposits representing those environments are only well exposed in the western basins. They have been too intensely resurfaced in the east basins.
Mineralogy of the Eridania basin
In this work, we analysed the infrared spectra of all Compact Reconnaissance Imaging Spectrometer for Mars (CRISM) and all High Resolution Imaging Science Experiment data within the Eridania basin in order to evaluate the detailed mineralogy and geological context of deep basin deposits within the Eridania region (Fig. 5).
CRISM spectra acquired of the kīpukas throughout the western and central Eridania basin contain absorptions at (λ) ∼1.4, 1.9 and 2.3 μm indicative of the presence of Mg-rich and Fe-rich clay minerals21,22 (Fig. 6). Fe-Mg-rich clays are common on Mars23,24, but in detail, the deep basin bedrock units show spectral characteristics unusual for the planet.
CRISM spectra of the kīpuka blocks typically show absorptions at 2.31–2.315 μm characteristic of Mg-rich, trioctahedral clay minerals. Specifically, this absorption is indicative of Mg3OH and Mg2FeOH combination bands in the octahedral sheets of saponite, talc, serpentine and various mixed-layer clays25. Pure talc (that is, with little Fe2+ or Fe3+ substitution for Mg2+) exhibits pronounced doublet absorptions at 2.29 and 2.31 μm, as do well-ordered examples of saponite and sepiolite.
The deep basin bedrock units show, in some cases, evidence for the doublet at 2.31–2.315 μm attributable to talc or other well-ordered, Mg-rich tetrahedral-octahedral-tetrahedral (TOT) clays such as sepiolite and some saponite, and in others, simply show a sharp absorption that could be attributable to saponite or Fe-rich talc. However, saponite and talc are commonly interstratified at the lattice scale in some seafloor settings26,27 (mixed-layering), and some of the best matches to these Martian spectra correspond to spectra of mixed-layer seafloor clays on Earth28. In addition, the presence of a 1.9 μm H2O absorption in many of the detections (Fig. 6) suggests the presence of TOT clays with expandable layers (smectite or smectitic mixed-layer clays). However its absence in other materials suggests non-expandable TOT clays, such as talc, or that expandable clays have been locally dehydrated while others remain hydrated. Absorptions at 1.39, 2.315, 2.43 and 2.51 μm in some deposits suggest the presence of serpentine29, which could also include serpentine-smectite mixed-layered clays (Fig. 6).
Fe-rich phyllosilicates are also observed. These deposits show absorptions at 2.295–2.305 μm, which are characteristic of Fe-rich dioctahedral mica or smectite with some Mg-substitution (that is, VIFe3+/Mg2+ molar ratio ≤4)28. Such materials are spectrally similar to Fe-rich seafloor deposits sampled on Earth, and easily distinguishable from Al-bearing nontronite formed in a subaerial/continental setting30. In some deposits, an unusual doublet absorption at 2.32 and 2.38 is observed, and the same spectra display a weak or absent 1.9 μm feature and a very strong spectral slope from 1 to 2 μm, indicative of Fe-rich serpentine- or chlorite-group minerals31. In fact, the 1–2 μm slope, which is stronger than is typically observed in Martian clays23 is likely a reflection of the abundant Fe2+ present in many of the clay detections32, and is a key indicator that the formation conditions likely involved a very Fe-rich fluid.
While the signature of phyllosilicates dominates the spectral character of the deep basin colles and chaos units, there are also several detections of jarosite occurring along with clay minerals within the chaos blocks (Fig. 6). The key distinguishing features of jarosite are absorptions at 2.265, 2.41, 2.46 and 2.51 μm (ref. 33). HOH absorptions occurring from 1.85 to 1.9 are variable on Mars34 likely due to K+, Na+ and H3O+ content33. The most common formation mechanism for jarosite is through oxidative chemical weathering of sulphide minerals35. Sulphides might be present in the deep basin units, but they are very difficult to detect directly because, in the near infrared, they exhibit few or no distinguishing features. In fact, jarosite formed through oxidative weathering36 is commonly considered a proxy for sulphide-bearing ore deposits35.
Spectra extracted from the central peaks and interior walls of impact craters occurring within the basin centres provide information about the mineralogy of the units stratigraphically below the Mg-clay units (for example, Fig. 4d), and other deposits at depth that are poorly exposed. A 17 km diameter impact crater in Caralis Chaos contains structurally and texturally complex blocks of exhumed bedrock in its central uplift that display spectral absorptions at (λ) ∼2.31 and 2.51 μm indicative of Mg-rich or Fe-Mn-Ca-Mg carbonate37 (Fig. 7). These materials also contain dense networks of crosscutting veins at the same scale (5–20 m-spacing) as is observed in the Mg-clay-bearing colles units (Fig. 7). Similarly, the central peak of an unnamed 15 km diameter crater in Ariadnes colles contains spectral evidence for Ca/Fe-carbonate in its central peak, as does a crater in the western, unnamed basin and the walls of a crater near Simois Colles where carbonates might have been mobilized within younger gullies38.
The carbonates might have formed from impact-generated hydrothermal activity, but they appear to occur within coherent bedrock exposed in the uplifted peak and rim (Fig. 7). Depth of exhumation can be assessed assuming that the central peak uplift represents a depth 10% of the final crater diameter39 (D=15–17 km in this case). The carbonates were likely uplifted from 1 to 2 km below the floor of the basin where the impact occurred, which has a Mars Orbiter Laser Altimeter (MOLA) elevation of −50 m. This observation suggests that alteration is present to substantial depth within the basin, the deep basin units might be kilometres thick, and that the phyllosilicate-rich deep basin units might overly or be interbedded with carbonate-rich rocks.
One ∼10 km diameter impact crater in Ariadnes Colles has exhumed material in its ejecta and rim that contain relatively strong absorptions at 1.9 and 2.24 μm indicating the presence of hydrated silica. But this crater is nested within a larger impact structure and it is possible that it has exhumed hydrothermal crater floor deposits formed from the earlier impact (Fig. 5).
Previous researchers identified chlorides in the region40 using data from the Thermal Emission Imaging System (THEMIS) (Fig. 5). In contrast to the Mg- and Fe-rich clays, which are concentrated below 300 m MOLA elevation, the chlorides occur at higher elevations (350–1,050 m) (Fig. 8). The average elevation of chlorides is 660 m, which is similar to the low-water level of the Eridania sea (700 m)13, suggesting they may have formed through evaporation in shallow seawater near the basin margin. Impact craters as small as 360 m-diametre have chloride-poor ejecta at distances up to 2–3 crater radii, suggesting that the craters have penetrated through a relatively thin (likely <30 m thick) chloride deposit (Fig. 8c).
Some of the eastern and northern parts of the basin contain Fe/Al-rich clays that are interpreted as pedogenic weathering sequences21, as has been observed elsewhere on Mars41,42. These deposits typically contain 2.28–2.29 μm FeFeOH and FeAlOH absorptions corresponding to aluminous nontronite, and in two cases contain absorptions at 2.2 μm corresponding to kaolinite-group clays and a broad absorption from 2.3 to 2.5 μm likely interpreted as polyhydrated sulphates43. In Eridania, these deposits occur in the superposed volcanic resurfacing unit and are therefore younger than and of different context to the deep basin deposits.
In previous works, many of the pedogenic-type deposits have not been delineated from the true deep basin deposits. Here we point out that the deep basin deposits are clearly distinguishable based on texture, colour, stratigraphic relations and mineralogy. The older deep basin deposits in the western basins contain clear and strong evidence for complex Mg- and Fe-rich clay mineralogy. The younger volcanic resurfacing units (Fig. 3d–f) are generally spectrally unremarkable. But it is in association with these units that pedogenic-type sequences are found.
Origin of deep basin deposits
The deep basin units in Ariadnes, Atlantis and Caralis basins formed in association with significant amounts of water, as evidenced by the presence of 100 s of metre thick deposits of phyllosilicates containing dense vein networks. It is possible that clay in Eridania could have formed in an alkaline-saline evaporative lake setting16,43, but we present challenges to the evaporite hypothesis, the most significant of which is the fact that the deep basin deposits are dominated by silicates rather than salt deposits.
The chemistry of the Eridania sea is unknown, though the volume to watershed ratio argues strongly that the sea was fed by groundwater13,15. Such a fluid would have been a Fe2+, Mg2+, Ca2+, Cl−, HCO3− and sulphur-rich-brine after interaction with the regional mafic-ultramafic crust44. Evaporation of such a fluid could initially produce Fe-carbonates. In fact, the occurrence of carbonates, exhumed from depth within the deep basin deposits is consistent with precipitation from an early phase of evaporation or freezing. But continuation along an evaporative pathway would quickly exhaust Fe2+ in solution leading to Mg-sulphate and ultimately to chloride precipitation45, which is not observed in the deep basin units. The deep basin deposits (that is, in the basin centres) contain >400 m thick clay deposits and no detectable hydrated sulphates or chlorides (Figs 5a and 8a), though anhydrite and small amounts of hydrous salts are possible.
Chlorides are present at higher elevations along the interior basin margins at concentrations 10–25% by volume46 and likely trace evaporitic, shallow water (<100 m) settings40. However, these deposits do not include any hydrated sulphates that should have precipitated before the chlorides during the evaporation sequence44,45. In most terrestrial playas, chloride deposits are situated in the middle of the basin rather than on the edges.
The lack of Mg, Fe sulphates in these deep basin deposits makes an evaporite-playa origin untenable. However, the chloride deposits on the basin margins may be related to evaporation in coastal, shallow water environments47. If the majority of the Eridania sea did not evaporate or freeze (both produce similar evaporite-type deposits), then the fluid was likely lost back into the subsurface due to some fundamental change in the regional groundwater table, perhaps including the formation of a new, deep basin that affected groundwater flow.
A detrital origin of clay-rich, deep basin deposits in Eridania is also unlikely. The concave topography of the deep basins below 700 m elevation is unusual for Martian basins13 (see Supplementary Fig. 2), most of which have flat floors that formed through subaerial resurfacing. The shape of Eridania basin floors argues strongly that the surfaces were protected below water13 during the period of intense sedimentary deposition on Mars (Late Noachian)11,48.
The deep basin deposits are unlikely to have formed by air fall as has been previously concluded12,16. The younger Electris deposits, which are layered, are of consistent thickness throughout the region (150–200 m), and occur at a wide range of elevations are consistent with an air fall origin49. By contrast, the deep basin deposits in Ariadnes and Atlantis are not layered, are thick, and concentrated at low elevations (Figs 5 and 8a). Ariadnes Colles and Atlantis Chaos contain at least 1–5 × 104 km3 of altered material (assuming a minimum thickness of 400 m and a likely thickness of >1 km). Deposition of such a thickness and volume of material is possible proximal to explosive vents50. It is possible that unrecognized volcanic vents are present51, but any air fall origin fails to account for why such thick deposits are found within the basins, but no trace of similar deposits of similar age are found outside the basins. Even if air fall deposition cannot be ruled out as a geological process, this model seemingly requires major volcanic source regions near, but outside the basins while ignoring the fact that volcanism would most likely be localized in the basins themselves, as is observed elsewhere on Mars and on other planets52.
The most plausible way to produce such large volumes of deep basin, deep water deposits is through seafloor volcanic-sedimentary processes focused in the basin floors where fractured, thinner crust and higher heat flow would be expected. Large volumes of Hesperian lava present throughout Eridania are proof that significant volcanism occurred within the basins. We argue that this volcanism did not suddenly begin after the sea had ceased to exist in the Early Hesperian, but most likely began in the Noachian, shortly after the basins formed. A sea of the size of Eridania is unlikely to have been ephemeral and therefore, it is nearly inescapable that subaqueous volcanism would have occurred during the period in which the sea existed.
Previous authors have demonstrated that most ancient, large impact basins on Mars were resurfaced by ultramafic to mafic volcanic materials—olivine rich lavas that have erupted through the relatively thin crust of basin environments53. The Eridania basins would have likely had the same type of activity. The important difference in Eridania is that a deep sea was present while volcanism occurred. If the Eridania sea level was at the 700 m elevation level (a conservative estimate), it implies that the deep basin deposits formed beneath 500–1,200 m water depth (Fig. 9). The lower gravity of Mars results in lower water pressure in a Martian sea compared to one on Earth, for a given depth (Fig. 9). Seafloor volcanism in Eridania would have occurred at water pressures of 20–50 bars. At these pressures, Martian seafloor volcanism could have included both effusive and explosive elements, in addition to chemical sedimentation from hydrothermal fluids (Fig. 10). The transition from altered deep basin deposits to flood lavas in the Hesperian does not represent the onset of volcanism in the basins, but the transition from subaqueous to subaerial volcanic activity as the Eridania sea came to an end.
Implications of the hydrothermal seafloor model
We conclude that thick, massive, clay-, carbonate- and likely sulphide-bearing deposits in Eridania basin formed in a deep-water hydrothermal environment on ancient Mars (>3.8 billion years ago) (Fig. 10). Saponite, talc, talc-saponite, Mg-bearing nontronite, glauconite, serpentine and berthierine are all common in terrestrial seafloor deposits26,27,54. The clay assemblages and spectral trends observed in seafloor deposits on Earth provide a good analogue for the deep basin deposits detected remotely in Eridania28. Salts only observed at higher elevations likely represent coastal evaporative settings (Fig. 10). Several lines of evidence strongly suggest that Eridania was a sustained inland sea in the late Noachian.
The deep-water environment was likely reducing based on direct evidence for Fe2+-rich clay minerals and indirect evidence for Fe-sulphides. This could be an indication of stratification of an ancient sea beneath an oxidized atmosphere, chemical isolation in an ice-covered sea, or quasi-equilibrium with a reduced atmosphere. The ancient Eridania sea deposits might represent a setting analogous to Fe-rich sea environments present on the early Earth.
Ancient, deep-water hydrothermal deposits in Eridania basin represent a new category of astrobiological target on Mars. To date, the search for habitable environments on Mars has been focused on exploration of ephemeral playa and shallow lacustrine settings. The Eridania deposits represent an ancient environment rich in chemical nutrients and energy sources. Such a deep-water environment would have been protected from harsh surface conditions and ideally suited for preservation of organic matter under reducing conditions. In fact, the earliest evidence of life on Earth seemingly corresponds to seafloor deposits2 of similar origin and age, although the terrestrial counterparts are metamorphosed and metasomatized. Eridania seafloor deposits are not only of interest for Mars exploration, they represent a window into early Earth.
Data required to complete this work include: (1) hyperspectral image cubes from CRISM; (2) high-resolution visible images from High Resolution Imaging Science Experiment; (3) day and night-time infrared image data from THEMIS; (4) visible image and digital elevation information from HRSC; and (5) topographic data from MOLA. All data used in this work, as well as the software used to process CRISM data, are available through the Planetary Data System (https://pds.nasa.gov). Other planetary data sets and visualization capabilities are available within the JMARS software provided by Arizona State University (https://jmars.asu.edu).
How to cite this article: Michalski, J. et al. Ancient hydrothermal seafloor deposits in Eridania basin on Mars. Nat. Commun. 8, 15978 doi: 10.1038/ncomms15978 (2017).
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Rosing, M. T., Rose, N. M., Bridgwater, D. & Thomsen, H. S. Earliest part of Earth’s stratigraphic record: A reappraisal of the >3.7 Ga Isua (Greenland) supracrustal sequence. Geology 24, 43–46 (1996).
Mojzsis, S. J. et al. Evidence for life on Earth before 3,800 million years ago. Nature 384, 55–59 (1996).
Ohtomo, Y., Kakegawa, T., Ishida, A., Nagase, T. & Rosing, M. T. Evidence for biogenic graphite in early Archaean Isua metasedimentary rocks. Nat. Geosci. 7, 25–28 (2014).
Manning, C. E., Mojzsis, S. J. & Harrison, T. M. Geology, age and origin of supracrustal rocks at Akilia, West Greenland. Am. J. Sci. 306, 303–366 (2006).
Irwin, R. P., Tanaka, K. L. & Robbins, S. J. Distribution of early, middle, and late Noachian cratered surfaces in the Martian highlands: implications for resurfacing events and processes. J. Geophys. Res. Planets 118, 278–291 (2013).
Connerney, J. E. P. et al. Tectonic implications of Mars crustal magnetism. Proc. Natl Acad. Sci. USA 102, 14970–14975 (2005).
McGovern, P. J. et al. Localized gravity/topography admittance and correlation spectra on Mars: implications for regional and global evolution. J. Geophys. Res. Planets 107, 5136 (2004).
Hahn, B. C., McLennan, S. M. & Klein, E. C. Martian surface heat production and crustal heat flow from Mars Odyssey Gamma-Ray spectrometry. Geophys. Res. Lett. 38, L14203 (2011).
Staudigel, H. Treatise on Geochemistry 2nd edn, Vol. 4 (eds Holland, H. & Turekian, K.), 583–606 (2013).
Taylor, G. J. et al. Variations in K/Th on Mars. J. Geophys. Res. 111, 1–20 (2006).
Fassett, C. I. & Head, J. W. Sequence and timing of conditions on early Mars. Icarus 211, 1204–1214 (2011).
Molina, A., de Pablo, M. Á., Hauber, E., Le Deit, L. & Fernández-Remolar, D. (Carlos). Geology of the Ariadnes Basin, NE Eridania quadrangle, Mars—1:1Million. J. Maps 10, 487–499 (2014).
Irwin, R. P., Howard, A. D. & Maxwell, T. A. Geomorphology of Ma’adim Vallis, Mars, and associated paleolake basins. J. Geophys. Res. Planets 109, E12009 (2004).
Hynek, B. M., Beach, M. & Hoke, M. R. T. Updated global map of Martian valley networks and implications for climate and hydrologic processes. J. Geophys. Res. 115, E09008 (2010).
Fassett, C. I. & Head, J. W. Valley network-fed, open-basin lakes on Mars: distribution and implications for Noachian surface and subsurface hydrology. Icarus 198, 37–56 (2008).
Adeli, S., Hauber, E., Le Deit, L. & Jaumann, R. Geologic evolution of the eastern Eridania basin: implications for aqueous processes in the southern highlands of Mars. J. Geophys. Res. E Planets 120, 1774–1799 (2015).
Howard, A. D. & Moore, J. M. Scarp-bounded benches in Gorgonum Chaos, Mars: formed beneath an ice-covered lake? Geophys. Res. Lett. 31, L01702 (2004).
Márquez, A., de Pablo, M. Á., Oyarzun, R. & Viedma, C. Evidence of gully formation by regional groundwater flow in the Gorgonum Newton region (Mars). Icarus 179, 398–414 (2005).
Michael, G. G. & Neukum, G. Planetary surface dating from crater size-frequency distribution measurements: partial resurfacing events and statistical age uncertainty. Earth Planet. Sci. Lett. 294, 223–229 (2010).
Hartmann, W. K. & Neukum, G. Cratering chronology and the evolution of Mars. Space Sci. Rev. 96, 165–194 (2001).
Noe Dobrea, E. Z., Moore, J., Howard, A., Catling, D. & Grant, J. Spectral and Geomorphic Evidence for a Past Inland Sea in Eridania Basin, Mars. Am. Geophys. Union http://adsabs.harvard.edu/abs/2008AGUFM.P32B..03N (2008).
Wendt, L., Bishop, J. L. & Neukum, G. Knob fields in the Terra Cimmeria/Terra Sirenum region of Mars: stratigraphy, mineralogy and morphology. Icarus 225, 200–215 (2013).
Carter, J., Poulet, F., Bibring, J. P., Mangold, N. & Murchie, S. Hydrous minerals on Mars as seen by the CRISM and OMEGA imaging spectrometers: updated global view. J. Geophys. Res. E Planets 118, 831–858 (2013).
Ehlmann, B. L. et al. Subsurface water and clay mineral formation during the early history of Mars. Nature 479, 53–60 (2011).
Cuadros, J., Michalski, J. R., Dekov, V. & Bishop, J. L. Octahedral chemistry of 2:1 clay minerals and hydroxyl band position in the near-infrared: application to Mars. Am. Mineral. 101, 554 LP-563 (2016).
Dekov, V. M., Cuadros, J., Shanks, W. C. & Koski, R. A. Deposition of talc—kerolite-smectite—smectite at seafloor hydrothermal vent fields: evidence from mineralogical, geochemical and oxygen isotope studies. Chem. Geol. 247, 171–194 (2008).
Cuadros, J. et al. Crystal-chemistry of interstratified Mg/Fe-clay minerals from seafloor hydrothermal sites. Chem. Geol. 360–361, 142–158 (2013).
Michalski, J. R. et al. Constraints on the crystal-chemistry of Fe/Mg-rich smectitic clays on Mars and links to global alteration trends. Earth Planet. Sci. Lett. 427, 215–225 (2015).
Ehlmann, B. L., Mustard, J. F. & Murchie, S. L. Geologic setting of serpentine deposits on Mars. Geophys. Res. Lett. 37, 1–5 (2010).
Bishop, J., Madejová, J., Komadel, P. & Fröschl, H. The influence of structural Fe, Al and Mg on the infrared OH bands in spectra of dioctahedral smectites. Clay Minerals 37, 607–616 (2002).
Calvin, W. M. & King, T. V. V. Spectral characteristics of Fe-bearing phyllosilicates: comparison to Orgueil (CI1), Murchison and Murray (CM2). Meteorit. Planet. Sci. 32, 693–701 (1997).
Bishop, J. L. et al. Phyllosilicate diversity and past aqueous activity revealed at Mawrth Vallis, Mars. Science 321, 830–834 (2008).
Bishop, J. L. & Murad, E. The visible and infrared spectral properties of jarosite and alunite. Am. Mineral. 90, 1100–1107 (2005).
Milliken, R. E. et al. Opaline silica in young deposits on Mars. Geology 36, 847–850 (2008).
Burns, R. G. & Fisher, D. S. Evolution of sulfide mineralization on Mars. J. Geophys. Res. 95, 14169–14173 (1990).
Burns, R. G. & Fisher, D. S. Rates of oxidative weathering on the surface of Mars. J. Geophys. Res. 98, 3365–3372 (1993).
Wray, J. J. et al. Orbital evidence for more widespread carbonate-bearing rocks on Mars. J. Geophys. Res. Planets 121, 652–677 (2016).
Korn, L. K. & Gilmore, M. S. in 46th Lunar and Planetary Science Conference Abstract #2224 (Woodlands, TX, USA, 2015).
Cintala, M. & Grieve, R. A. F. Scaling impact melting and crater dimensions: Implications for the lunar cratering record. Meteorit. Planet. Sci. 33, 889–912 (1998).
Osterloo, M. M., Anderson, F. S., Hamilton, V. E. & Hynek, B. M. Geologic context of proposed chloride-bearing materials on Mars. J. Geophys. Res. E Planets 115, E10012 (2010).
Noe Dobrea, E. Z. et al. Mineralogy and stratigraphy of phyllosilicate-bearing and dark mantling units in the greater Mawrth Vallis/west Arabia Terra area: Constraints on geological origin. J. Geophys. Res. 115, 1–27 (2010).
Carter, J., Loizeau, D., Mangold, N., Poulet, F. & Bibring, J. P. Widespread surface weathering on early Mars: a case for a warmer and wetter climate. Icarus 248, 373–382 (2014).
Pajola, M. et al. Eridania Basin: an ancient paleolake floor as the next landing site for the Mars 2020 rover. Icarus 275, 163–182 (2016).
Catling, D. C. A chemical model for evaporites on early Mars: possible sedimentary tracers of the early climate and implications for exploration. J. Geophys. Res. 104, 16453 (1999).
Tosca, N. J. & McLennan, S. M. Chemical divides and evaporite assemblages on Mars. Earth Planet. Sci. Lett. 241, 21–31 (2006).
Glotch, T. D., Bandfield, J. L., Wolff, M. J., Arnold, J. A. & Che, C. Constraints on the composition and particle size of chloride salt-bearing deposits on Mars. J. Geophys. Res. Planets 121, 454–471 (2016).
Deocampo, D. M. & Jones, B. F. Geochemistry of Saline Lakes 2nd edn,Vol. 7 (eds Holland, H. & Turekian, K.), 437–469 (2013).
Fassett, C. I. & Head, J. W. The timing of martian valley network activity: Constraints from buffered crater counting. Icarus 195, 61–89 (2008).
Grant, J. A. et al. HiRISE views enigmatic deposits in the Sirenum Fossae region of Mars. Icarus 205, 53–63 (2010).
Kerber, L., Head, J. W., Madeleine, J. B., Forget, F. & Wilson, L. The dispersal of pyroclasts from ancient explosive volcanoes on Mars: implications for the friable layered deposits. Icarus 219, 358–381 (2012).
Michalski, J. R. & Bleacher, J. E. Supervolcanoes within an ancient volcanic province in Arabia Terra, Mars. Nature 502, 47–52 (2013).
Greeley, R. & Spudis, P. D. Volcanism on Mars. Rev. Geophys. 19, 13–41 (1981).
Edwards, C. S., Bandfield, J. L., Christensen, P. R. & Rogers, A. D. The formation of infilled craters on Mars: evidence for widespread impact induced decompression of the early Martian mantle? Icarus 228, 149–166 (2014).
Nimis, P., Tesalina, S. G., Omenetto, P., Tartarotti, P. & Lerouge, C. Phyllosilicate minerals in the hydrothermal mafic–ultramafic-hosted massive-sulfide deposit of Ivanovka (southern Urals): comparison with modern ocean seafloor analogues. Contrib. Mineral. Petrol. 147, 363–383 (2004).
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Michalski, J., Dobrea, E., Niles, P. et al. Ancient hydrothermal seafloor deposits in Eridania basin on Mars. Nat Commun 8, 15978 (2017). https://doi.org/10.1038/ncomms15978
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