Ceres is a partially differentiated dwarf planet, as confirmed by NASA’s Dawn mission. The Urvara basin (diameter ~170 km) is its third-largest impact feature, enabling insights into the cerean crust. Urvara’s geology and mineralogy suggest a potential brine layer at the crust-mantle transition. Here we report new findings that help in understanding the structure and composition of the cerean crust. These results were derived by using the highest-resolution Framing Camera images acquired by Dawn at Ceres. Unexpectedly, we found meter-scale concentrated exposures of bright material (salts) along the crater’s upper central ridge, which originate from an enormous depth, possibly from a deep-seated brine or salt reservoir. An extended resurfacing modified the southern floor ~100 Myr after crater formation (~250 Myr), long after the dissipation of the impact-generated heat. In this resurfaced area, one floor scarp shows a granular flow pattern of bright material, showing spectra consistent with the presence of organic material, the first such finding on Ceres beyond the vast Ernutet area. Our results strengthen the hypothesis that Ceres is and has been a geologically active world even in recent epochs, with salts and organic-rich material playing a major role in its evolution.
The dwarf planet Ceres is the largest (~940 km diameter) object in the main asteroid belt, orbiting the Sun at a mean distance of ~2.8 astronomical units. Ceres is a survivor of the earliest period of Solar System formation and thus detailed knowledge about its interior provides fundamental insights into the formation and evolution of volatile-rich planetary embryos that originated within the protoplanetary disc1. Findings of the Dawn mission2 suggest that Ceres’ interior consists of a thin lag deposit (regolith) layer, an icy crust (density3 ~1.3 g/cm3) containing the bulk of an ancient ocean, a relict brine layer at the crust-mantle transition, and a lower mantle (<100 km depth, density ~2.4 g/cm3) that is presumably dry and coherent4. A denser core, if present, could not be sensed by the gravity data5.
The Framing Camera6 (FC) and the Visible and Infrared Spectrometer7 (VIR) of the Dawn mission revealed local evolutionary processes in surprisingly recent epochs, for example at the Occator crater, where cryovolcanism shaped the cerean surface8,9. Less apparent are similar indicators at older sites, which are more affected by erosion, surface relaxation and ejecta blanketing. However, it is suggested that among larger impacts, Occator-like late activity was prevalent and is possibly still traceable through the analysis of the highest spatial resolution FC imagery. The FC imaged the cerean surface in seven colour filters and one clear filter (0.4–1.0 µm), leading to a global colour filter mapping at a pixel scale of ~140 m during the High Altitude Mapping Orbit (HAMO) and at a ~35 m pixel scale for the clear filter during the Low Altitude Mapping Orbit (LAMO)10,11. In addition, during its extended mission phase 2 (XM2), clear filter images of Urvara were obtained with a pixel scale down to ~3 m, and these are analysed here for the first time. From the VIR, we added infrared (IR) spectral information obtained in the wavelength range 1.0–4.1 µm at a spatial scale of ~95 m from the LAMO. Details about the data acquisition and calibration can be found under Methods (‘Data processing’).
In this work, we present a detailed analysis of high-resolution imaging data of the Urvara basin. We find metre-scale exposures of bright material (salts) along its upper central ridge, which originate possibly from a deep-seated brine or salt reservoir. The southern floor shows an extended resurfacing of about 100 Myr after the impact (~250 Myr before today), which is long after the dissipation of the impact-generated heat. In this younger area, one-floor scarp exhibits a granular bright material flow that shows spectra consistent with the presence of organic-rich material. This is the first finding of organic-rich material outside the Ernutet area and its surroundings. Our results strengthen that Ceres is a geologically active world where salts and organic-rich material play a major evolutional role.
Geology of Urvara basin
One of the largest impact structures on Ceres is the Urvara basin at 45.66°S/249.24°E (Fig. 1a, b), located at an average altitude of about −6100 m below the reference ellipsoid12, and thus it is one of the lowest-lying surface areas. It may have formed within a larger, ancient eroded basin that had a north-south extent of ~240 km. This ancient basin is indicated by a discontinuous circle of elevations, which resemble a second, heavily eroded wall (Supplementary Fig. 1). The older Yalode basin (Fig. 1a) to Urvara’s east has likely also influenced its pre-impact geology.
In general, Urvara’s morphology is consistent with a complex, medium-aged impact crater, exhibiting a preserved ejecta blanket to its west. The basin exhibits a sharply defined continuous crater wall with vast terraces, caused by post-impact inward slumping, in its south, while a steep single scarp defines the northern and north-eastern rim (Fig. 1b). The wall shows a significant height variation (Supplementary Fig. 1). The sharpness of the northern wall gradually declines towards the east, allowing it to be overtopped by ‘smooth material’ (SM). Numerous small craters pepper the SM, but larger relief is missing. The origin of the SM at Urvara is important, since it is one of the major geologic units on Ceres, and is younger than the crater13. Urvara’s location at the transition between the smoother equatorial zone and rougher higher latitudes likely influenced the different morphology of the northern and southern crater walls. The differences in topographic roughness on a global scale indicate the diversity of conditions during the evolution of Ceres’ surface. Detailed descriptions of the geology and mineralogy of Urvara using lower-resolution images already exist13,14,15,16, hence the present paper focuses on observations of brine residues using high-resolution images.
A central ridge is located off-centre (Fig. 1b) and rises ~3 km above the southern floor (Supplementary Fig. 2). The ridge marks the highest part of an extended topographic step, separating the elevated northern from the southern floor. The northern flank of the central ridge declines gradually, whereas its southern flank is steep (average slopes up to ~75°), exposing fragmented bedrock (cliffs) followed downwards by a smooth sloped talus that is peppered by numerous boulders (Fig. 2). The cliffs consist mainly of indurated blocky material, extending 300 m below the crest, and exhibit inclusions of bright material (BM) indicative of salts that originate from great depth. In addition, very coarse meso-boulder17 production proximal to the cliff faces occurs. Many of these boulders tumbled down the talus slope (leaving trails) and accumulated at the base of the central ridge. The presence of meso-boulders and talus suggests that the cliff-forming material is compositionally heterogeneous. The meso-boulders represent a mechanically stronger component that can survive attrition as they tumble down the slope, while the talus represents a mechanically weaker component that erodes away with ease into finer-grained particles and may serve as a matrix material. The mechanical strength of the boulders points to either a certain degree of cementation or their inherent strength. The nature of these cliffs is of importance since they exhibit inclusions of BM possibly originating from a deep source.
Urvara crater contains a central ridge. Central ridges are common features of larger cerean craters, with prominent examples being found in Haulani and Achita. Central ridges are expected to form due to oblique impacts18,19 or, alternatively, they could be remnants of collapsed central peaks. The orientation of Urvara’s central ridge may indicate an oblique impact from the south-west19. However, the different morphology between the north-east and south-west crater wall is due to differences in the crustal properties between the southern and equatorial latitudes rather than being caused by an oblique impact, since Yalode shows a similar difference. Moreover, the ejecta field appears symmetrical13, not showing ‘forbidden zones’ as would be expected in the case of an oblique impact18. Furthermore, the circular outline of the crater wall is improbable for very oblique impacts20. Therefore, we conclude that Urvara’s central ridge is likely the remnant of a collapsed central peak and is hence expected to uplift and expose materials from the deep interior.
Eastward of the central ridge, we identified a central pit (~20 km diameter, 0.56 km deep) in the basin’s average topographic profile (Fig. 3). Central pit craters on Ceres are rare9 and demand a high volatile content of the crust. The Dp/Dc ratio, in which Dp is the diameter of the central pit and Dc is the (IAU) diameter of the crater, is 0.12. This value fits well within the range of ratios (0.06–0.25) found for cerean pit craters21. The model age of the pit (Area 13, see Supplementary Tables 1, 2) is consistent with Urvara’s formation age, suggesting a nearly concurrent formation of the crater and the central pit as expected from crater mechanics. Central pits form in complex craters on various planetary bodies but are more frequent on volatile-rich objects, such as the icy moons of the outer Solar System22. Central pits are an indication of high volatile content in the subsurface at the time of impact21,23 and thus are consistent with water ice and the potential presence of brines in the subsurface. Barlow21 favours a combination of the ‘central peak collapse’ model24,25 and the ‘layered target’ model26 for explaining the development of central floor pits. Pit formation occurs, according to the first hypothesis, via the collapse of a central peak into a void created by the gradual release of impact-induced volatiles or the drainage of impact melt. The second hypothesis adds the importance of a layered target surface, a stronger surface over a weaker substrate. The global stratigraphy of Ceres matches a stronger surface (crust) that overlays a weaker mantle27 and thus would be consistent with the second hypothesis. A combination of both these hypotheses could also explain the formation of Urvara’s central pit. Thus, the presence of a central pit supports our hypothesis of a partially collapsed central peak capable of revealing subsurface materials.
Except for some portions of the northern floor, which display a rugged topography (see geologic map13), the floor is dominated by units of SM, whereas in the north and north-east SM even extends across and beyond the crater rim. The SM also appears to blanket older floor units and terraces. Isolated elevations protrude through the SM, especially in the eastern half of the floor. The elevations south-east of the ridge could also be remnants of a former central peak or rough original floor material, which were embayed by impact slurries. Knobby elevations, bay-like features at the outermost contacts to the crater wall and even inside the floor resemble buried craters, which were formed by flow fronts of solidifying impact slurries.
Several linear grooves traverse the eastern and western floor (see Supplement), which could be indicative of post-impact horizontal and vertical movements of the SM and thus could suggest late floor activity, possibly caused by cryovolcanism, late outgassing or/and severe mass wasting.
One of the deepest areas in Urvara is an undulated, irregular unit south of the central ridge (Supplementary Fig. 2), characterised by numerous shallow depressions described as a ‘pitted texture’14. Some of these depressions (≤2 km) are only partially developed and show no ejecta or elevated rims akin to impact craters. This terrain indicates the past outgassing of a volatile-rich subsurface, which is in line with the appearance of a central pit. However, flow features28 that could be indicative of volatiles have not been found.
Distinctive colour and spectral features
The colour variation of Ceres’ surface proved to be significantly stronger than expected, in terms of both reflectance and spectral shape. For example, young craters often show deposits of BM but also display significantly darker exposures than average (e.g. ejecta)11. This spectral diversity demonstrates that Ceres is not a simple agglomeration of materials of uniform composition, but has undergone complex evolutionary processing. Local occurrences of BM are globally present on Ceres. All of these BMs consist of salts as hyperspectral investigations show29. Due to their characteristic spectral shape in the FC wavelengths, salty BM can also be identified by using colour images. The bright material on Ceres is often associated with impact craters30, but some instances exist where it is associated with mons31 or volcanic features9. Understanding the nature, occurrence and distribution of BM on Ceres enables us to draw conclusions on a deep global brine layer, which bears key implications for the cerean evolution models.
Urvara shows a distinctive spectral diversity, much greater than the neighbouring Yalode basin. Figure 4 displays a newly calibrated and processed false-colour mosaic (RGB), with a considerably improved photometric correction of topography. Several colour units can be distinguished. Increased content of BM, whose reflectance is defined as being larger than 0.035 at 0.55 µm32, raises the overall reflectance of the central ridge area, the rugged terrain and extends beyond the western crater rim. Material darker than Ceres’ average is mainly restricted to the eastern part of the floor.
The dark bluish material has a relative reflectance higher than the cerean average at 0.44 μm (Fig. 4, units (4) and (5)). This material often shows a reflectance peak at 0.55 μm, is associated with a number of small impact craters, and is found on the SM as well as Urvara ejecta.
The comparatively high reflectance at 0.44 µm seems linked with freshly exposed material since all these craters appear morphologically uneroded and unit (4) is young (see the section ‘Crater-based model ages’). However, dark bluish craters also exist on old SM. Thus, their bluish appearance may relate to ejecta freshness and physical regolith parameters rather than the composition and absolute age of the geologic unit in which they formed.
Spectrally, the younger and older SM (see the section ‘Crater-based model ages’) appear similar at IR wavelengths. The smooth material is found at many other localities on Ceres, is associated with larger impact craters and is the equivalent to solidified impact melt33,34, although its granularity and depth are unknown.
Exposures of BM, characterised by their isolated occurrences and sharp contrast with their surroundings (Fig. 2 and Supplementary Fig. 3), display reflectances up to ~0.08 at 0.55 µm and at a ~140 m pixel scale. These exposures have been detected on the upper central ridge of Urvara. We refer to these exposures as ‘CREs’ (Central Ridge Exposures). The brightest CREs are associated with a cliff at the north-east central ridge (Fig. 2b). They exhibit colour spectra similar to the average cerean BM (see ‘Urvara CRE (#1)’ spectrum in Fig. 5). The CREs’ colour spectra (Fig. 6) differ from those of Occator’s faculae, suggesting different salt compositions. Significantly higher reflectances have been measured among XM2 data at pixel scales <5 m. Metre-scale concentrations of BM, associated with a cliff on the north-east central ridge (Fig. 2b and Supplementary Fig. 3), exhibit reflectances up to ~0.16 in the clear filter; these are comparable to those measured for Occator’s Vinalia Faculae, indicating high concentrations of salts. Further CREs are found along the ridge, and all are exposed by slumping, mainly on the southern ridge scarp, excavating lenses of BM, which mixes with darker material while moving downslope.
In order to test either common or unique nature of the CREs, we performed a survey of all central peak/ridge craters on Ceres. In total, 239 potential or secure central peak/ridge craters have been identified, but only about 16 of these show BM on their central peaks/ridges at a ~35 m pixel scale. Exposures of BM on central peaks/ridges were found at craters larger than ~25 km in diameter, with Urvara being the largest. Thus, the occurrence of BM on central peaks/ridges for craters >25 km seems to be rather independent of crater size and therefore of the local depth of excavation. Bright exposures on central peaks/ridges are found over a wide range of ages, from young craters like Haulani (~1.96 Myr, LDM)35 to Urvara, which is more than 100 times older. However, their detectability tends to decay with age, possibly due to an alteration of brine residues as they are exposed to the space environment30.
Setting a minimum reflectance threshold of 0.05 (at 0.55 µm) we find additional outcrops of BM on the northern and north-western upper crater wall, also exposed by slumping. However, the extent of their total area is relatively small compared to other cerean craters, like, for example, Haulani36. The colour spectra of Urvara’s bright wall exposures (not shown) reveal that most of these comprise only a minor content of BM, since their spectral shapes are similar to those of the dark background material, but with a slightly higher overall reflectance. Only a few BM wall exposures exhibit the typical reflectance peak at 0.55 µm that is characteristic of cerean BM. A prominent example is found on the eastern crater rim at 40.05°S/260.41°E (‘BM terrace (#4)’, Fig. 5a). Here, a number of bright dots pepper the upper scarp of a terrace, possibly exposed or deposited by a small impact. A further site is found on the western rim at 42.19°S/237.08°E, where a crater of 1.1 km diameter exposes BM with a reflectance of up to 0.07 (at 0.55 µm and at a ~140 m pixel scale). A few small BM sites are also found on Urvara’s floor. Most of them exhibit colour spectra, similar to the dark floor but with higher reflectances. However, some of these units show colour spectra similar to the average BM spectrum of Ceres (Fig. 5). Examples are located at 49.18°S/244.36°E (‘BM floor (#6)’, Fig. 5a) and at 42.19°S/237.06°E (‘BM floor (#5)’, Fig. 5a). In both cases, craters ≤ ~0.75 km diameter are associated with these deposits. Another site of ~70 m in size is located on the north-eastern floor (38.41°S/255.42°E, ‘BM floor (#3)’, Fig. 5a), showing a reflectance of 0.044 (at 0.55 µm and at a ~140 m pixel scale). The highest spatially resolved image shows a tiny bright patch, concentrated in a single FC pixel (pixel scale ~33 m) with some brightness-enhanced radially deposited material in its vicinity, resembling a rayed crater.
Surprisingly, a site of ~0.1 by 0.5 km in size on the western floor at 46.53°S/243.26°E (Fig. 7) has different spectral characteristics. This site exhibits an overall red-sloped spectrum in the FC wavelength range without the typical reflectance peak at 0.55 µm of cerean BM outside Occator (see ‘Urvara red-sloped site (#2)’, Figs. 5a, 6) and thus deviates significantly from all other BM in Urvara. As Fig. 6 demonstrates, the site shows a colour spectrum that is similar to those of organic-rich material found in and around the Ernutet crater37, but differs from the colour spectra of Cerealia Tholus9,38. High-spatial-resolution XM2 imagery reveals that this spectrally red-sloped (reddish) site is located on a scarp on which the BM moves downslope (Fig. 7). This scarp is part of the rugged terrain bordering the young smooth floor material. The BM seems to discharge from the outer (slumping) wall of a small impact crater of ~100 m diameter. The reflectance of the reddish material reaches 0.13 in the clear filter at a pixel scale of ~3–5 m, i.e. its reflectance is similar to the lower reflectances measured for Occator’s faculae but higher than the reddish sites associated with Ernutet, which exhibit typical reflectances of ~0.035. Further BM exposures on other nearby scarps exhibit typical average cerean BM spectra, i.e. they show a reflectance peak at 0.55 µm but no spectral reddening along the FC spectrum. The question arose as to whether the reddish BM contains organic material as the color spectra suggest. To address this, we compared the VIR IR spectra of the reddish BM in Urvara with the spectra of reddish material at Ernutet and BM at Cerealia Tholus (Fig. 8). In VIR data at a ~0.4 km pixel scale, the reddish BM site is barely resolved, i.e. only a few pixels cover the bright flow. As Fig. 8 demonstrates, the IR spectrum of the reddish BM site deviates significantly from that of Cerealia Tholus. The latter exhibits two prominent absorption features at ~3.5 and ~4.0 µm related to sodium carbonate, which are absent in all the other spectra. Thus, the reddish BM in Urvara is of a different composition to the BM of Cerealia Tholus. Next, we verified whether the compositions of the reddish material at Ernutet and the reddish BM in Urvara could be similar. As Fig. 8 shows, both these spectra exhibit similarities. Both display an absorption feature at ~3.4 µm, although the feature is weaker for the reddish BM in Urvara. A ~3.4 µm feature can be diagnostic for organics if it is stronger than a potential ~3.9 µm absorption, while a stronger ~3.9 µm and a weaker ~3.4 µm are diagnostic for carbonates39. Thus, we conclude that Urvara’s reddish BM likely contains organics. In addition, we found a distinct but weaker ~3.4 µm feature combined with slightly red-sloped FC spectra in the immediate vicinity of the reddish BM. This could indicate a wider distribution of organics on this scarp.
Crater-based model ages
The probability distribution of our measured ages (see also ‘CSFD model ages’ and ‘CSFD areas’ under Methods), showing four peaks, is presented in Fig. 9. The thick curve is the sum of all thin curves, which represent the individual ages (Supplementary Tables 1, 2). The broad peak at ~250 Myr represents the formation age of Urvara, in line with previous results40,41. This peak comprises several ages (areas 2 A/B, 3, 4 A/B/C, 7, 8, 9, 16 and 17; Fig. 10 and Supplementary Fig. 4) belonging to different geologic units, including the ejecta. The probability peak exhibits a shoulder towards higher ages that is likely caused by secondary impacts, which pepper in particular the north-eastern part of Urvara. A further well-defined peak at ~160 Myr (formed by areas 1 A/B, 5, 6, 10, 11 background and 15) indicates a prominent resurfacing, affecting a continuous area of smooth material on the southern floor and adjacent areas. This finding is remarkable because one would expect the entire floor to show the same age, which is close or equal to the crater formation age. However, we find a difference of ~100 Myr between the crater formation age and the southern SM. The reliability of the age difference (see also ‘Robustness of model ages’ under Methods) is supported by flow fronts at the border between the young and older smooth material (Supplementary Fig. 5). Counting Area 10 matches the ‘pitted terrain’ described in the section ‘Geology of Urvara basin’. A peak at ~20 Myr in Fig. 9 belongs to a local resurfacing event affecting Area 11, which otherwise shows a background age of ~170 Myr, in agreement with the adjacent young smooth material. Area 11 corresponds to the talus of the scarp shown in Fig. 7, associated with the reddish site (Figs. 5a, 6). Here resurfacing is likely caused by mass wasting(s) on a steep slope. The well-defined peak at ~8 Myr represents the formation age of the dark bluish crater on the north-western crater rim (see Fig. 4 and previous section).
Urvara’s pre-impact crustal stratigraphy must have been altered by the putative ancient basin and the Yalode impact, reducing its volatile content and influencing the peculiar distribution of floor colours/materials. While geologic units contemporary with the formation of the crater can be attributed to crater mechanics, other units like the pitted terrain, the rugged terrain that hosts the scarp showing the reddish material, and the younger smooth material are influenced by post-impact modifications. The measured time difference of ~100 Myr is much longer than the period required for impact slurries to solidify and impact melt chambers to refreeze. Thus, the question arises as to which process could be responsible for the major resurfacing affecting the floor.
The central ridge exposes the deepest materials in Urvara, probably from a depth down to ~50 km42,43 below the pre-impact surface. Evidence for such a deep excavation, apart from the large diameter of Urvara, is the enrichment of ammoniated phyllosilicates in the central area44. The age of the northern flank of the central ridge (Area 9, Fig. 10) is, within uncertainties, consistent with the crater formation age and thus congruent with both potential hypotheses of origin (see the section ‘Geology of the Urvara basin’). Deposition of the CRE material by secondary projectiles at its exceptional, isolated location is very unlikely; an explanation by an in situ origin is mandatory. Among those, a near-surface origin of the CREs is not likely, since the areas’ specific impact history must have led to a severe mixing of materials and a depletion of local crustal volatiles. These findings narrow down the possibilities of CRE origin. One potential explanation is that the BMs were uplifted from great depths when the central peak formed. According to numerical modelling of impact cratering processes42,43, material from a depth of about 0.5 to 0.7 crater radii can get exposed in a central peak, i.e. the Urvara impact could have reached the potential global brine layer at a depth of ~40 km9,45,46,47. The question is whether frozen or liquid brines from the crust-mantle transition would survive an uplift during the central peak formation to the near-surface and would leave behind intact salt lenses within the central peak, since the uplift leads to severe heating, shattering and deformation of the material. An alternative explanation for the origin of CREs is cryovolcanism. The transport of brines from depth could have started when extended crustal cracks formed during the impact or later through crustal shrinking due to the cryomagma chamber refreezing. These cracks could have connected a deep-seated brine reservoir with the surface. Then the exsolution of gases at depth could have led to the ascent of brines. The presence of gases at depth is inferred from the composition of Occator’s faculae, which are rich in sodium carbonate. If brines migrate towards the surface, only two principal possibilities exist for separating the water from the dissolved salts: (1) cryovolcanism: on reaching the surface brines start to boil, water is lost to space immediately, salt crystals form, and are deposited on the surface; later on they are covered and mixed with darker material; (2) subsurface intrusion: brines do not reach the surface but reside at near-surface depths. Solvent loss is achieved by capillary transport of brines through the porous upper crustal material; brines possibly solidify upon cooling and releasing water into space through sublimation of the icy component leaving behind salts. The contribution of carbon dioxide to such volatile activity cannot be quantified, since there is no corresponding remnant, although the presence of carbonates is a strong relevant indication.
If the proposed mechanisms were truly responsible for the CRE formation, it should also explain the related phenomena in the surrounding floor. Subsurface cavities/porosities filled with brine (and its residues) might have formed the CREs and possibly also subsurface floor BM. Similar processes are described for the Occator crater9,38,45,47 in which bright extensive salt deposits document cryovolcanic activity, well beyond the epoch of the formation of the crater, and a link between the cerean surface and a deep-seated brine reservoir. However, it remains to be explained why evaporites occur mainly on the central ridge rather than on the floor. The relatively low number of BM exposures on the floor rather tends to negate surface volcanism, but former salt deposits could have been wiped out by severe mixing and irradiation. We did not find spectrally reddish material among the CREs, which could be a consequence of a time-dependent decay of such a spectrally red component (organics) due to the higher age of Urvara. In summary, a cryovolcanic activity that did not reach the surface seems more likely to us for Urvara.
The clearest hint of volatile activity is the presence of sublimation or devolatilization pits on a low-lying floor area (Supplementary Fig. 2). Violent outgassing of the aqueous vapour phase must have occurred ~100 Myr years after crater formation (Area 5, Fig. 10), confirming the former presence of significant volatile content in the subsurface, outlasting the violent impact history. In our interpretation, due to the release of volatiles, the pre-surface of the “pitted terrain” subsided to the current elevation level and caused instabilities and small-scale collapses. Thus, it seems that these volatiles were involved in a resurfacing that completely reset the cratering record in the southern floor. Hence, the observed morphology supports the cryovolcanic interpretation.
Smooth material covers different units (see ‘Geology of Urvara basin’) and three hypotheses of origin have been suggested13: (1) localised extrusions of volatile-rich material; (2) remobilisation of the volatile-rich rim and/or terrace materials; and (3) deposits from Yalode and Urvara that have merged together to form a single unit (fallback material). Hypothesis 1 could explain the formation of the young SM, although no source vents are seen. However, the old SM is spread over different elevations and thus an extrusive origin seems unlikely. Hypothesis 1 also has the difficulty of explaining by which process (energy source) the younger SM could have extruded ~100 Myr after the formation of the crater. Possibly, cryomagma formed and extruded in a similar process to that suggested for Titan48. Resurfacing on Titan is explained by occasional cryovolcanism, caused by cracking at the base of the ice shell and formation of liquid pockets in the ice— somehow similar to the predicted situation in the cerean lower crust. Hypothesis 2 would require a late large-scale event, triggering remobilisation of the wall and terrace material. Such an event could be a large near impact, causing instabilities of the crater wall and terraces. However, whether this could lead to extended floor flooding and resurfacing of adjacent elevated areas is highly debatable. No indication of such an outer influence is detectable. Hypothesis 3, in which fallback ejecta form the SM, is inconsistent with ejecta modelling, since only a minor fraction of the ejecta returns to its source crater49. Moreover, the younger age of several SM units does exclude the fallback hypothesis. On the other hand, the similar age of the younger SM and the pitted terrain indicate a link and the possibility that both formations could have been caused by one event. However, the case is different for the western floor, where significant amounts of BM are admixed over a wide area. This BM was possibly directly excavated from the lower crust by the impact, whose transient crater must have reached the brine layer at a depth of ~40 km. Again, the multiple instances of BM demonstrate the presence of a brine/salt layer before the impact. Regardless of whether the formation of the CREs occurred due to an uplift process during the central peak formation or through late cryovolcanism, the presence of liquid or frozen brines or their remnants at great depth is required for explanation and supported by evidence. Thus, we conclude that brine/salt layers at different depths exist in the cerean crust or even form a single layer, which shows a varying depth. However, the intense bombardment of Ceres by large projectiles during its evolution, including the ancient impact mentioned above, could have caused a local thinning, depletion, or even destruction of an ancient deep-seated brine layer, reducing the amount of detectable BM in Urvara.
The presence of organic material in Urvara, the first detection outside the Ernutet area, is enigmatic and significant. Its sensitivity to spectral degradation by space weathering50 may be responsible for its scarcity. The exposure in Urvara resembles a representation of a similar distribution of the organic material as in the Ernutet region: comparably small in extent and confined to low depth. The organic absorption at 3.4 µm and the red-sloped FC spectra extend to the immediate vicinity of its brightest location. It seems that this brightness represents the purest form of the organics in terms of concentration and its pristine status as a very fine-grained bright deposit. As in Ernutet, there is no obvious sign of a fresh local impact justifying exogenic infall as a source of origin. However, the spectral properties of the reddish material are distinct from those of salty BM. Due to the sensitivity of the organic material to alteration, its presence in the impact-heated and resurfaced floor of Urvara is remarkable. It raises questions on the carbon chemistry of Ceres’ crustal or deeper materials and points to a much more widespread distribution during earlier epochs of Ceres’ evolution.
Our results on Urvara prove, as for Occator9, a post-formation activity, causing resurfacing of a significant fraction of Urvara’s floor ~100 Myr after crater formation, i.e. long after the dissipation of the impact heat. The organic-rich material on a relatively young floor scarp is independent of an impact origin. In addition, the CREs are hard to explain without liquefaction. However, a deep brine layer may enable resurfacing, fresh salt deposits, and the injection of organic material from below. Our findings strengthen the view of a dwarf planet, which is a recently geologically active world, where salts play a prime role in preserving liquids in a heat-starved body.
Dawn’s FC imaged the surface of (1) Ceres from several different orbits between 2015 and 2018. Global mapping in seven bandpass and one clear filter has been achieved from Survey, HAMO and LAMO orbits at pixel scales of ~400, ~140 and ~35 m, respectively, whereby LAMO colour data were restricted to a number of high-priority surface features, excluding Urvara. After completing its primary mission phase at Ceres, Dawn was extended twice (XM1 and XM2 mission phases), leading to further colour and clear filter mapping with often similar spatial resolutions to those during the prime mission. However, in June 2018, the spacecraft entered its final elliptical orbit, enabling spatial resolutions of the Occator and Urvara regions of a magnitude better than before (pixel scale up to ~3 m). This clear filter imagery of Urvara in combination with the colour data of the prime mission (HAMO) of the same region have been analysed in the present work.
The calibration of the FC imagery is detailed in a number of publications and project reports51,52. Images exist at different processing levels: 1a (raw), 1b (radiometrically corrected) and 1c (stray light and ghost-image corrected). We used the highest corrected data51 level 1c, which is converted to reflectance (I/F) by dividing the observed radiance by the solar irradiance from a normally solar-illuminated Lambertian disk. All used mosaics and colour cubes are computed by an extensive USGS ISIS script45,53, involving a photometric correction to standard viewing geometry (30° incidence, 0° emission angle, and 30° phase angle) using Hapke functions54. Hapke light scattering parameters have been iteratively derived from the Approach, Survey, and HAMO mission phases, starting from parameters obtained by ground-based observations55. Iteration of these parameters became necessary because increasing image resolution leads to the increasing significance of sub-pixel shadows, which change the weight of contributions from different latitudes to a globally integrated model fit. For example, a transition from a one-parameter Henyey-Greenstein function to a two-parameter description56 was required for the HAMO data. For the photometric correction and the visualisation of our mosaics, we used the HAMO Ceres shape model deduced from FC clear filter stereo images57. Alternatively, especially for the higher-resolution data, we computed stereo digital terrain models (DTMs) from LAMO and XM2 clear filter imagery by using the Ames stereo pipeline58 or used the LAMO SPC shape model59. The resulting reflectance data are map-projected in several steps, and co-registered to align the colour frames, creating mosaics/colour cubes for further analysis.
The uncertainties of the presented reflectances are based on measurements of homogeneous areas in different mission phases and illumination geometries for which various measurement box sizes were analysed60,61.
CSFD model ages
Our approach to estimating absolute surface model ages is based on the analysis of crater size-frequency distribution (CSFD) measurements62. The underlying chronology model for our analysis is based on the link between radiometrically dated lunar surface samples brought back by sample return missions (Apollo, Luna) and the measured CSFDs of the related geologic units on the Moon63,64,65. The lunar chronology system has been converted to the impact conditions on other bodies such as Mercury, Mars and main belt asteroids66. The conversion from the lunar chronology system to the lunar-derived Vestan chronology system has been tested successfully for the cases of basin formation ages on Vesta and radiometrically dated Vestan meteorites that recorded those energetic events66. The cerean chronology system and its relation to the lunar chronology system was detailed previously67. In order to derive meaningful ages, it is required to measure crater frequencies on geological units that were formed by a specific process at a specific time68. Within a geologic unit, each subarea should show the same result. Uncertainties of model ages are influenced by statistical and parameter uncertainties as well as uncertainties caused by geologic conditions9.
Robustness of model ages
For Occator small differences of ~4 Myr in crater retention ages between its ejecta blanket and its crater floor have been linked to uneven material properties that allowed the same projectiles to create slightly larger craters in the lower-strength ejecta material9,69. The same cause has been considered for the measured age difference on the floor of Urvara. In order to explain the observed age difference of about 100 Myr, the craters in the younger unit would need to be about 14% smaller than those craters in the older unit, which is similar to comparable observations on the Moon70. However, in contrast to the Moon and Occator crater, in Urvara the age differences occur within the floor of Urvara with lower retention ages constrained to the south-eastern part of the crater floor. It is not immediately clear to us why the material properties should change while the floor morphology remains similar. In fact, the region where the change in crater retention ages occurs shows lobate morphology, implying a quasi-fluid deposition of a layer superposing the existing crater floor. Digital Elevation Models (DEMs) from high-resolution stereo images suggest layer thicknesses of at least a few decametres up to more than 100 m. One example of such a lobate layer is presented in Supplementary Fig. 5. Since none of our CSFD measurements in the younger smooth unit appears to show a resurfacing kink that would support a superposing thin layer erasing only the smaller craters, we conclude that all craters that formed during the ~100 Myr between crater floor formation and the emplacement of the superposing smooth layer were completely erased. From our crater chronology model, we believe that between one and two 1 km craters should have formed in our respective measurement areas during that time, which have been erased. These numbers increase by the power of three, going to smaller crater diameters (N∝D-³).
We mapped craters in Area 10 with increased attention, such that pits are excluded, as they do not bear any age information. Misclassification of pits into craters would lead to an overestimation of the surface age.
Figure 10 presents an overview of all analysed areas, which can roughly be subdivided by their location. Areas 14, 16 and 17 dates the formation of crater ejecta blankets. While Areas 16 and 17 dates the formation of the Urvara ejecta and thus the formation of Urvara itself, Area 14 dates the formation of a dark bluish 8-km-diameter crater on the north-western crater rim of Urvara. Areas 2 A/B, 4 A/B and 7 are located in the terraced area of Urvara. Usually, these terraces form shortly (minutes to days) after the crater formation. Thus, these areas give a minimum age for the formation of Urvara. Areas 1 A/B, 3, 4 C, 5, 6, 8, 9, 10, 11, 13 and 15 represent different sections of the crater floor and can signal post-formation resurfacing events as has been shown in the Occator crater9. Area 11 is the smallest area investigated and follows the foot of a scarp in which mass wasting may occur, for instance, due to seismic shaking. Usually, such areas are avoided for surface age determination because of reoccurring mass wasting events, but in this case, our goal was to date an event that may have happened at the scarp in conjunction with the exposure of the spectrally reddish material.
The Framing Camera and VIR data are available through the PDS Small Bodies Node website (https://pds-smallbodies.astro.umd.edu/). Higher data products that support the findings of this study are available from the corresponding author upon reasonable request.
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We thank the Dawn mission team for the development, cruise, orbital insertion, and operations of the Dawn spacecraft at Ceres. Also, we would like to thank the instrument operations teams at MPS and INAF. The Framing Camera project is financially supported by the Max Planck Society and the German Space Agency, DLR.
The authors declare no competing interests.
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Nathues, A., Hoffmann, M., Schmedemann, N. et al. Brine residues and organics in the Urvara basin on Ceres. Nat Commun 13, 927 (2022). https://doi.org/10.1038/s41467-022-28570-8