The Pleistocene presence of the genus Homo in continental Southeast Asia is primarily evidenced by a sparse stone tool record and rare human remains. Here we report a Middle Pleistocene hominin specimen from Laos, with the discovery of a molar from the Tam Ngu Hao 2 (Cobra Cave) limestone cave in the Annamite Mountains. The age of the fossil-bearing breccia ranges between 164–131 kyr, based on the Bayesian modelling of luminescence dating of the sedimentary matrix from which it was recovered, U-series dating of an overlying flowstone, and U-series–ESR dating of associated faunal teeth. Analyses of the internal structure of the molar in tandem with palaeoproteomic analyses of the enamel indicate that the tooth derives from a young, likely female, Homo individual. The close morphological affinities with the Xiahe specimen from China indicate that they belong to the same taxon and that Tam Ngu Hao 2 most likely represents a Denisovan.
From the Early to Late Pleistocene, the presence of Homo erectus is well documented in Asia, notably in China and Indonesia1,2,3. However, the taxonomic attribution of most Asian late Middle Pleistocene Homo specimens remains a matter of contention4,5,6,7. The recent description and analysis of the Harbin cranium from China has reignited this debate by suggesting its attribution to a new species named Homo longi8, but this new taxonomic attribution remains highly debated. In fact, the Harbin cranium shows close morphological similarities with other late Middle to early Late Pleistocene Asian Homo specimens from Dali, Xujiayao, Xuchang and Hualongdong, whose taxonomy remains unclear4,9,10. These fossils are considered to belong to a different taxon than H. erectus and are often grouped under the generic label ‘archaic humans’9,10. Due to the combination of features they exhibit, including Neanderthal-like traits, it has been suggested that they belong to an Asian sister taxon of Neanderthals, the Denisovans, even if this attribution remains under debate5,11,12. The small number of fossils currently securely attributed to the Denisovans (Denisova 2, a lower left molar; Denisova 3, a distal manual phalanx; Denisova 4, an upper left M3; Denisova 8, an upper molar; and the Xiahe mandible)13,14,15,16 prohibits a clear morphological picture of their overall morphology. The geographic distribution of the Denisovans also remains debated. Modern Papuans, Aboriginal Australians, Oceanic/Melanesian, Philippine Ayta groups and, to a much lesser extent, mainland Southeast Asian populations, retain a Denisovan genetic legacy14,17,18,19. Combined paleoproteomic and morphometric analyses recently suggested that the Middle Pleistocene Xiahe mandible from Baishiya Karst Cave belonged to a Denisovan, extending the known range of this group onto the Tibetan Plateau15. However, there is still no fossil evidence explaining the Denisovans genetic imprint on modern southeast Asian populations and—due to the paucity of the Middle Pleistocene fossil record—it is still unknown whether one or more human lineages (co)existed in continental southern Asia. We present here to the best of our knowledge the first unambiguous Middle Pleistocene Homo specimen from mainland southeast Asia and discuss its taxonomic attribution and implications for human evolution in the region.
In December 2018, a hominin permanent lower molar was recovered from a breccia block at Tam Ngu Hao 2 (Cobra Cave), Huà Pan province, Laos (20°12′41.5′′N, 103°24′32.2′′E, altitude 1,116 m; Fig. 1, Supplementary Fig. 1). The tower karst in which the cave was formed is positioned on the south-eastern side of P’ou Loi Mountain with an entrance located 34 m above the alluvial plain (Fig. 1a, Supplementary Fig. 1). The site was discovered during a survey of the area around Tam Pà Ling, where early Homo sapiens fossils have previously been recovered20,21,22. The tooth (TNH2-1) is a mandibular left permanent molar crown germ (Fig. 2a–f; Supplementary Fig. 2), and the absence of occlusal and interproximal wear combined with the incipient root formation suggests that the tooth was unerupted at the time of the individual’s death. The morphology of the tooth is compatible with an attribution to either a first or a second lower molar (Methods-Detailed morphological analysis of the tooth). In either case, considering the early maturational stage of the root, this tooth belonged to a juvenile individual corresponding to an age ranging from 3.5 to 8.5 years following modern developmental standards23.
In this work to best document THN2-1, morphological description and comparative analyses are performed. We also develop a specific sampling protocol that allows us to sample for palaeoproteomic and future isotopic analyses while preserving the whole occlusal surface morphology of the crown. Sampling for these destructive analyses takes place after microCT analysis of the entire tooth, ensuring full morphological data were saved. No additional sampling for ancient DNA analyses is performed at this stage given the old age of the specimen and the tropical conditions under which the sediment and fossils were deposited. The invasive sampling strategy to collect dental tissues for molecular analyses only focuses on the distal part of the inferior aspect of the crown, keeping the mesial portion of the crown intact.
Context and dating
The geological setting, stratigraphy and micromorphology of the sediment sequence were analysed to obtain a comprehensive, multi-scalar assessment of the depositional context and taphonomic history of the fossils recovered from the cave (Supplementary Information, Geology). The partially eroded sediments that infill the studied entrance passage comprise a lower and an upper facies representing two phases of sediment accumulation separated by an erosional surface and an unknown period of time (Fig. 1b). The lower facies (Lithological Unit 1, LU1) is weakly cemented and forms an arenitic silty clay deposit that is devoid of fossils (Fig. 1e). The upper, fossiliferous facies (Lithological Unit 2, LU2) is well cemented and coarse grained, containing intrakarstic angular limestone clasts and extrakarstic rounded pebbles, forming a very hard breccia/conglomerate layer from which skeletal elements—and in particular, teeth—were recovered in high frequencies (Fig. 1d). The change in lithology between the two facies most likely reflects a reconfiguration of the karstic hydrological system as would be associated with a major flood, eroding space in LU1 onto which the sediments of LU2 were unconformably overlain. The sediments of LU2 are laterally contiguous and densely packed throughout the exposure excavated for this study, precluding major reworking of material and confirming the stratigraphic context of the fossils contained within, including the hominin tooth (see detailed observations described in Methods). The upper facies (LU2) is draped with two carbonate flowstones, indicating a final change in hydrology and the passage of surface water out of the cave and the precipitation of laminar speleothem (Fig. 1c).
Three bovid teeth (TNH2-10/CC10, TNH2-11/CC11, TNH2-12/CC12) recovered from the upper fossil-bearing breccia (LU2) were directly dated using coupled uranium series and electron spin resonance (US-ESR), providing a weighted mean age estimate of 151 ± 37 thousand years ago (kyr) (2-sigma) (Fig. 1b; Supplementary Tables 1, 2) and an age range of 188–117 kyr. Two large blocks of breccia (LCC1 and LCC2) from LU2 (upper) and one block of the silty clay unit (LCC3) from LU1 (lower) were removed for luminescence dating (Fig. 1b). These samples produced coeval age estimates of 143 ± 24 kyr (LCC1) and 133 ± 19 kyr (LCC2) for the deposition of the LU2 breccia and 248 ± 31 kyr (LCC3) for the underlying LU1 silty clay deposit (Supplementary Table 3). These ages are in stratigraphic agreement with the age of the overlying flowstone (CCF1), which was precipitated earlier than 104 ± 27 kyr based on the weighted mean of U-series age estimates on four separate sub-samples of flowstone carbonate (Supplementary Table 4). Bayesian modelling was performed on all independent age estimates to determine an overall geochronological framework for the site and tooth (Methods and Supplementary Fig. 3). The fossiliferous breccia including the tooth was deposited between 164 and 131 kyr (at 68% confidence limit).
The Tam Ngu Hao 2 faunal assemblage comprises 186 identified dentognathic specimens (NISP) dominated by isolated teeth of large mammals, including several megaherbivores (Supplementary Table 5, Supplementary Data 2). Their analyses reveal typical taphonomic pathways of assemblages from karstic systems in terms of representation of specimens and types of damage. Due to the energy associated with the deposition of LU2, only teeth of large mammals are present in the assemblage, and we note the absence of small and light teeth of any microvertebrates. Moreover, most teeth are gnawed by porcupines, known to be a major accumulator agent in the region24. Therefore, the poor preservation of specimens precludes identification to the species level for most of the recorded taxa. The fauna bears close affinities to those known from the late Middle Pleistocene of southern China and northern Indochina and, to a lesser extent, Java, which is consistent with the sedimentary chronology of the site. It can be assigned to the “Stegodon-Ailuropoda faunal complex”25,26,27,28. We note the absence of Neogene taxa that persist in the Early Pleistocene and that of two key-species, Pachycrocuta brevirostris and Gigantopithecus blacki, which are good indicators of pre-300 kyr faunas in the region26,27,29,30,31. The archaic Stegodon persisted in Asia most likely until the end of the Late Pleistocene32. We recovered herbivores including Tapirus, Stegodon, and Rhinocerotidae, that were adapted to canopied woodlands in the area. We also found animals such as the Bos species, small-sized Caprinae and large-sized Cervidae (possibly Rusa unicolor), which are all known to exhibit a great variability in their feeding behaviour and preferred habitats, from closed and intermediate forests to open grassland33.
Ancient protein analyses
The enamel from the TNH2-1 tooth specimen was analysed using nanoLC-MS/MS and the recently developed approach for ancient enamel proteomes34. The TNH2-1 proteome is composed of a common set of enamel-specific proteins, all of which have previously been observed in Pleistocene enamel proteomes34,35,36 (Supplementary Table 6). The enamel proteome has elevated levels of diagenetic protein modifications (Supplementary Fig. 4a–d, Supplementary Table 7) and preserves serine (S) phosphorylation within the S-x-E motif previously observed in ancient dental enamel34,35 (Supplementary Fig. 4e). Based on proteome composition and modification, as well as the absence of peptides matching any of these proteins in our extraction and mass spectrometry blanks, we consider our proteomic data as indicative of endogenous proteins deriving from the sampled enamel.
Unfortunately, no high-confidence peptides overlapped diagnostic amino acid positions with sequence differences between H. sapiens, Denisovans, or Neanderthals, making further taxonomic assignment based on palaeoproteomics impossible. This is in line with previous research, which indicated that closely related hominin populations can be distinguished based on dentine and bone proteomes, while enamel proteomes are less informative in the context of close phylogenetic proximity35. Nevertheless, by comparing the sequences recovered from the TNH2-1 enamel proteome with that of extant hominids for which protein sequences are available, we find that the specimen belongs to a member of the genus Homo (Supplementary Table 8).
The absence of peptides specific to male-diagnostic amelogenin Y (AMELY) suggests that either the sampled molar was from a female individual or that AMELY-specific peptides were not observed due to degradation beyond the limit of detection of the instrument.
External and internal structural analyses of the tooth
Externally, the TNH2-1 crown displays a coarse wrinkling pattern that is found in Pleistocene Homo (H. erectus s.l., European and Asian Middle Pleistocene Homo and Neanderthals), but is rare in modern H. sapiens. The mid-trigonid crest is well developed as commonly recorded in European Middle Pleistocene Homo and Neanderthals, while it is generally absent or less frequent in H. erectus s.l. and fossil and extant H. sapiens37. Below the external surface, the enamel-dentine junction (EDJ) of the tooth shows the dentine horns of the five main cusps and of a tuberculum intermedium and a low but uninterrupted mid-trigonid crest (Figs. 2 and 3, Supplementary Fig. 2; Methods). The latter feature is generally found in Neanderthals (80–100% depending on the molar position)38,39,40 but is less frequent in H. erectus s.l. and H. sapiens41,42,43,44,45,46,47 (Supplementary Fig. 5). In addition, the EDJ of TNH2-1 shows an internally-positioned metaconid reminiscent of Neanderthal molars40 and a low crown topography similar to that of H. erectus41,42,43,44,45,46,47. These features, as well as a slight buccal shelf present on the EDJ of TNH2-1, are all expressed on the EDJ of the Denisovan molars from Baishiya Karst Cave (Xiahe, Gansu, China) (Supplementary Fig. 5)15. TNH2-1 dentine differs from the much higher and proportionally more mesiodistally compressed EDJ of Neanderthals and H. sapiens39,40, as well as from the shorter dentine horns and more densely wrinkled occlusal basin of H. erectus s.l.41,42,43,44,45,46,47 (Supplementary Fig. 5).
In terms of absolute dimensions, only Asian Middle Pleistocene Homo have larger tooth crowns than TNH2-1 (Supplementary Tables 9, 10). TNH2-1 crown metrics are within the ranges of variation for H. erectus s.l., H. antecessor, Asian Middle Pleistocene Homo and Neanderthals, but they statistically differ from the smaller crowns of European Middle Pleistocene Homo and from Pleistocene and Holocene H. sapiens (Fig. 4; Supplementary Tables 10, 11). With respect to tooth crown tissue proportions, TNH2-1 has a high percentage of crown dentine (Vcdp/Vc: 55.37%) with moderately thick enamel as shown by absolute and relative enamel thickness values (3D AET: 1.18 mm; 3D RET: 17.00; Supplementary Table 12). These crown tissue proportions match to those of the nearly unworn M2 of the Xiahe mandible15 (Vcdp/Vc: 54.62%; 3D AET: 1.47 mm; 3D RET: 18.97) and the upper molar of Denisova 4 (3D RET: 15.27; B. Viola, pers. comm.), but within the ranges of variation of all comparative fossil and extant human groups (Supplementary Fig. 6a–c; Supplementary Tables 12, 13). Three-dimensional maps of topographic enamel thickness distribution show that TNH2-1 has the thickest enamel at the top of the hypoconid and hypoconulid cusps and in the distobuccal quarter of the crown (Supplementary Fig. 6d). In comparison, all other samples tend to have the thickest enamel distributed on all buccal cusps and more spread on the buccal aspect of the crown, even if variable between groups and between molar positions. The M2 of the Xiahe specimen shows thicker enamel spread along the buccal crown aspect but its distribution pattern is partly obliterated by occlusal wear.
The EDJ shape of TNH2-1 was quantitatively compared with those of Pleistocene and Holocene human groups using geometric morphometrics (Methods). Landmark-based and surface deformation-based approaches were used, with both methods similarly distinguishing between H. erectus s.l., European Middle Pleistocene Homo and Neanderthals and H. sapiens using canonical variate and between-group principal component analyses (Fig. 5, Supplementary Fig. 7). Along CV2 and bgPC1, the higher EDJ and more externally set dentine horns of Neanderthals and H. sapiens are discriminated from the lower and more centrally positioned dentine horns of H. erectus molars. The CV1 and bgPC2 axes separate Neanderthals from modern humans, with the former having more internally placed mesial dentine horns and a more developed hypoconulid than the latter. TNH2-1 falls outside the ranges of all other groups. It has an intermediate EDJ shape between the low crown of H. erectus (but exceeding the variation of the latter group along CV1 and bgPC2) and the cusp position of Neanderthal molars (even if outside their range of variation along CV2 and bgPC1). TNH2-1’s closest morphological affinity lies with the Denisovan specimen Xiahe, which also displays Neanderthal-like features (Fig. 5, Supplementary Fig. 7).
Reconstructing dispersals and ultimately evolutionary trajectories of Homo in Asia depends on a currently poor fossil record. The Asian late Middle Pleistocene fossil record is mostly limited to the eastern part of the continent4,8,9,10,15,48. Any additional human remains from this time period documenting the evolution of Homo in southern Asia might thus help confirm previous hypotheses or reveal new lineages. Proteomic analysis of the TNH2-1 molar indicates that it most probably belongs to a female individual of the genus Homo. Morphometric analyses of the external and internal crown structural organisation allow us to reject a number of hypotheses regarding species assignment. TNH2-1 has large crown dimensions and a complex occlusal surface that differentiates it from the smaller and morphologically simpler teeth of H. floresiensis49, H. luzonensis50 and H. sapiens (Fig. 4). The EDJ shape shows a mixture of Neanderthal-like and H. erectus-like features, closely resembling the M1 morphology of the Denisovan specimen from Xiahe (Fig. 5, Supplementary Fig. 5). The similarities between TNH2-1 and H. erectus are mostly related to the proportionally lower crown, although H. erectus molars display even lower molar crowns and a narrower occlusal basin (Figs. 2 and 3, Supplementary Fig. 5). The Lao fossil shows clear Neanderthal-like features such as a well-developed mid-trigonid crest and internally-positioned mesial dentine horns, but differs with its much lower EDJ topography and occlusal basin shape.
The differences from Neanderthals that we observe do not preclude TNH2-1 from belonging to this taxon and would make it the south-eastern-most Neanderthal fossil ever discovered. However, considering the morphological particularities of TNH2-1 in unison, as well as the high-degree of morphodimensional similarities with the molars of the Denisovan specimen from Xiahe, the most parsimonious hypothesis is that TNH2-1 belongs to this sister group of Neanderthals. If TNH2-1 indeed belongs to a Denisovan, this occurrence, along with the recent discovery of a Denisovan mandible from the Tibetan Plateau, a high-altitude, hypoxic environment15, would suggest that this Pleistocene Asian population possessed a high degree of plasticity to adapt to very diverse environments51. Available Denisovan dental remains indicate a mixture of traits consistent with the current paleogenetic evidence that Denisovans and Neanderthals are sister taxa13,14,51,52,53 and are therefore expected to share some craniodental features15,54. This is further supported by recent analyses that identified possible Denisovan skeletal characteristics based on unidirectional methylation changes including traits that have been linked to Chinese fossils such as Xujiayao and Xuchang9,54. Denisovans are notable for their large dentition, with some Neanderthal-like crown features15,48,54, as well as distinctive cusp and root morphology14,15,16. In the absence of molecular analyses, looking for these combined features in the Asian human fossil record, including in fossils like the Penghu 1 mandible from the Taiwan Strait55, may help identify more Denisovan specimens (Supplementary Fig. 8).
The alternative hypothesis that TNH2-1 belongs to a group of Neanderthals that made an incursion into southeast Asia (see for example discussions on fossils that may demonstrate this dispersal from Maba and Dali)56,57 cannot be outright rejected, even if it is less likely.
The tooth from Tam Ngu Hao 2 Cave in Laos thus provides direct evidence of a most likely Denisovan female individual with associated fauna in mainland Southeast Asia by 164-131 kyr. This discovery further attests that this region was a hotspot of diversity for the genus Homo (Supplementary Fig. 8), with the presence of at least five late Middle to Late Pleistocene species: H. erectus58, Denisovans/Neanderthals, H. floresiensis49, H. luzonensis50 and H. sapiens20,21,22.
Fossiliferous breccia has been extracted mecanicaly from the walls of the cave and some of the hardest blocks containing the fauna have been disolved within a 10% formic acid solution.
Excavation, collection, export of fossils for study have been granted by the Ministry of Information, Culture and Tourism of Lao PDR in January 2019 with the support of the local authorities of Xon district, Hua Pan Province and the villagers of Long Gua Pa village. Results of this study will be shared with the authorities of Xon District and with the villagers of Long Gua Pa village, following the same information routine we set up at the beginning of each of our annual fieldworks.
For the purposes of analysing the microstratigraphy of the Cobra Cave sediments, an intact sediment block was removed from LU1 (MM1) and LU2 (MM2) (Fig. 1b). The unconsolidated sample (MM1, LU1) was extracted using a gypsum-impregnated bandage to stabilise the sediment. It was possible to remove the sample from LU2 (MM2) using a hammer and chisel because of the well-cemented nature of the breccia. The sample from LU2 was located in an area close (~30 cm) to the hominin tooth find-spot. Thin sections were prepared at Adelaide Petrographics (Adelaide, Australia). The block from LU2 did not require stabilisation and was cut using a rock saw. A ~100 µm slice was mounted on a glass slide and ground and polished down to a final thickness of 30 µm. The sediment block from the lower unconsolidated unit was impregnated with resin, following procedures described elsewhere59,60. Diagnostic features observed using a polarising microscope were recorded for each layer using standard protocols61.
Micromorphological (microstratigraphic) analyses of cave sedimentary infills can elucidate the processes responsible for the formation of a fossil site, the depositional and post-depositional environments, and the context of fossil assemblages59,60,62,63,64. Micro-contextualisation can provide critical information regarding the context of fossils and how far they may have travelled from their original positions.
LU1: Lower sands and silts (Supplementary Fig. 9a)
The lower sediments of LU1 appeared sandy and gritty in the field, but microstratigraphic analyses show that the sand-sized inclusions comprise silty clay aggregate grains of variable lithological composition. These lower sediments are generally loose but with partial cementation in localised zones. In broad terms, the sediments of LU1 (Supplementary Fig. 9a) consist of i) a matrix material of fine quartz sand in a speckled b-fabric and ii) large, coarse, sand-sized, rounded to well-rounded aggregate grains with variable colour, lithology and fabric arrangement, suggesting polygenetic (intra and extrakarstic) origins.
Groundmass ranges from single-spaced to double-spaced enaulic. At the macro-scale, the compound grains form the coarse fraction of the overall sediment, ranging from very fine gravel/very coarse to fine sand and in shape from angular to well rounded. The coarse component of the matrix material comprises very fine quartz sand and coarse silt, sub-angular to sub-rounded. Many of these aggregate grains exhibit internal stratification with micro-banding of finer and coarser material (primarily clay and silt), and grains vary in colour from pale brown to very dark brown. The sediments are moderately porous, exhibiting frequent planar, vughy and vesicle voids. Planar voids generally link vertically or sub-vertically across vughs and vesicles and are common adjacent to the edges of large compound grains. Stratified compound grains are generally much less porous and are often clay-enriched. Pedofeatures are rare in LU1 and are most commonly evident in the form of clay pendent coatings surrounding rounded to sub-rounded compound grains. Small ferrous particles are present in small quantities. Organic material is absent from this layer.
Field observations and micromorphological analyses together suggest that LU1 was deposited in a low to moderate energy hydrological environment. The coarse nature of the aggregate grains (very fine gravel, very coarse sand and ranging down to fine sand) suggest that water flowing through the karstic system reworked older cave fills adhered to the walls and roof higher up the cave catchment system (cf.62). The variable lithologies of these compound grains are consistent with reworking of fine-grained material from multiple sources, most likely of both intra- and extra-karstic origin. The very dark coloration of some (≤5%) of the aggregate grains suggest either reworked pedogenic material or pelite sourced from outside the site. Following deposition of these fossil-sterile sediments, minor post-depositional disturbance of the sediments occurred, evidenced by the well-developed void structure consistent with bioturbation. Bioturbation has contributed to the removal of any banding, laminations or structures diagnostic of specific fluvial sedimentation processes.
LU2: Upper fossiliferous conglomerate/breccia (Supplementary Fig. 9b–t)
As stated above, the conglomerate was sampled to avoid gravel clasts and so this description pertains to the fine sediment matrix. Randomly distributed void spaces are present, with common very small vughs and planar voids, which are locally larger and more complex, sometimes forming chamber and channel voids. All void spaces are infilled with calcium carbonate to cement the sediment. Groundmass is generally a double-spaced porphyric c/f distribution pattern with frequent angular to sub-angular mineral grains (mainly quartz), small angular fragments of bone, large tooth fragments and some small (fine to medium sand-size) iron-stained nodules. Fabric is infrequently granostriated around coarse inclusions (e.g., quartz or rock grains). Pedofeatures are rare in the TNH2 cave sediments but infrequent clay coatings are recorded in some areas of the examined thin section, with thin coatings on some bone fragments. There are also regions where the sediment matrix is clay-enriched, probably the result of illuviation. Bone fragments are typically medium to coarse sand-size in thin section (with larger elements recovered from the sediment) and exhibit only moderate signs of chemical weathering, with low birefringence (in xpl) and some signs of oxide staining probably related to microbial activity. In some regions of the sample, small bone fragments are particularly weathered and exhibit small cracks and heavy oxidation, and these might therefore represent older, lag deposits. Large tooth fragments (~15 mm in size) are present, including both dentine and cementum in a well-preserved state.
The sediments of LU2 comprise fine to medium gravels, coarsening up to large gravel clasts and occasional cobbles in towards the upper capping flowstone. The gravel is suspended in a fine-grained matrix of silts and fine to medium sands, with variable quantities of clay. These sediments were deposited in a high energy environment, probably during a flood event or reconfiguration of the karst hydrogeological system. This probably occurred as a single event in the course of hours or days as we do not identify sub-units, potentially as both fluvial discharge and saturated debris flows. Mass movements are recorded in the microstratigraphy as granostriated b-fabrics surrounding coarse mineral grains, evidence that (rotational) pressure has been applied around grains. These sediments were probably water saturated and plastic, with percolating water translocating fine clays through the profile concentrating these fines in localised regions of the matrix, as recorded in localized regions of the sampled sediments.
Micromorphological analyses confirm field observations that small bone fragments and frequent large tooth fragments are common throughout the sampled area of LU2, indicative of a long residence time in the karstic network. The bone fragments are commonly angular retaining aspects of their original morphology and are generally well-preserved with the exception of moderate iron staining consistent with microbial action. In terms of the diagenetic and taphonomic signature recorded in these sediments, there is scarce evidence of acid etching or edge rounding of the organic components, although some quartz grains do exhibit weathering features. Only very few bone fragments (<5%) show signs of significant weathering consistent with longer storage time in the karstic network. Although we record small-scale bioturbation of the sediments, this is minor, and the void spaces created are not of sufficient size to be the source of mixing of the sediments.
Luminescence dating of breccia matrix
Two large blocks of the hard-cemented, fossil-bearing breccia (LCC1 and LCC2) from LU2 and one from the lower silty clay unit (LCC3) in LU1 were cut from the sections in situ and wrapped in black plastic (Fig. 1b). Within subdued red-light conditions, the light-exposed, outer layer was removed using a chisel and hammer and was retained as the dosimetry sample. These layers were broken up using a pestle and mortar and oven dried, then the entire fraction was milled and used for environmental dose estimation. The unexposed inner core was also broken up using a pestle and mortar and was processed using the standard sample purification procedures for feldspar separation65 including a 10% wash in hydrofluoric acid for 10 min to remove the external alpha-dosed rinds58. All luminescence analysis was conducted at the ‘Traps’ luminescence dating facility at Macquarie University in Sydney, Australia.
Individual 180–212 µm feldspar grains were mounted onto coated, single grain discs in a 10 × 10 grid. The discs were loaded onto a carousel and processed in a Riso TL-DA-20 containing an automated Detection and Stimulation Head set up with a Dual laser single grain attachment with a Blue/UV sensitive Electron Tube PMT (PDM9107Q-AP-TTL-03) with maximum detection efficiency between 200 and 400 nm. The filters in the automated detection changer were set on the blue filter pack (Schott BG-39 and Corning 7–59 filters to transmit wavelengths of 320–480 nm66. The grains were stimulated using an IR (830 nm) 140 mW TTL modulated laser with a 3 mm RG-780 longpass filter (mounted directly in front of the IR laser), and the emissions were detected using the blue filter combination described above. The laser stimulated the grains for 2.5 s, first at 50 °C and secondly at 270 °C, after a 300 °C preheat according to the procedures of the pIR-IRSL protocol67 (see Procedural tests below). The single-grain disc locating process was programmed to occur before any disc heating procedure to ensure that each grain received the same heating within the SAR cycles.
Equivalent doses were corrected according to the results of the anomalous fading tests (using a weighted mean fading rate of 2.0 ± 0.2% per decade) then run through a minimum age model (MAM) to identify the population that had the most bleaching prior to burial.
To obtain an estimate of the environmental dose rate for each of the samples, we first measured beta dose rates using a Geiger-Muller multi-counter beta counting of dried and powdered sediment samples68 in the laboratory. Allowance was made for the effect of sample moisture content, different grain sizes69 and HF etching on attenuation of the beta dose, and the total beta dose-rate contribution was calculated by comparing the beta count rate to a standard beta source (SHAP with a dose rate of 5.99 Gy/kyr) and magnesium oxide as a non-beta emitting background material. Secondly, thick source alpha counting using a Daybreak 583 intelligent alpha counter was used to obtain estimates of Uranium and Thorium70 to estimate the gamma dose rate, and thirdly the difference between beta and alpha counting was used to estimate potassium values. These estimates were then converted to gamma dose rates using the conversion factors of Guerin et al71. Allowance was made for the effect of sample moisture content65 on the external beta and gamma dose rates using a long-term water content of between 3 ± 0.2–5 ± 2%, which is similar to the measured (field) water content of between 3% and 7% and allows for an initial period of saturation when first deposited in the karst environment.
The total dose rate was then calculated using an effective internal beta dose rate of 0.84 Gy kyr−1 72,73 for the 180–212 µm feldspar samples (due to the radioactive decay of 40K and 87Rb), which were made assuming K (12.5 ± 0.5%) and 87Rb (400 ± 100 μg g–1) concentrations and included in the total dose rate. Cosmic-ray dose rates were estimated from published relationships74, making allowance for the thickness of limestone above the cave (~20 m with an assumed density of 1.2 g/cm3), sediment overburden at the sample locality (0.3–1.3 m with an assumed density of 2.0 g/cm3), the altitude (~1116 m above sea level) and geographic latitude and longitude (20°S and 103°E) of the sampling site.
In addition, this estimation of dose rates was supported by high resolution gamma spectrometry to measure the activities of radionuclides in the 238U, 235U, 232Th decay chains and of 40K at the SGS laboratory in Melbourne. These activities were converted to beta and gamma dose rates using the conversion factors of Guerin et al.71 and adjusted for the same long term water content as mentioned above. These activities provide an alternate dosimetry and were also used to estimate the potential disequilibrium in this cave environment.
Previous luminescence analyses at a neighbouring site, Tam Pà Ling20,21,22, revealed high dose rate (~3–4 Gy/kyr), a saturating quartz signal with depth >4 m and feldspars with a high dose response and stable signal that could be isolated from the unstable fading signal22. Building on this experience, we focused on just the feldspars and applied the same post-infra-red infra-red-stimulated-luminescence (pIR-IRSL) protocol to overcome the problems of anomalous fading75. However, due to the number of feldspar grains used on each disc, which produced only maximum ages for sediment deposition, combined with a low yield in potassium feldspar grains at these sites, we decided to apply a single-grain pIR–IRSL technique rather than the single aliquot technique.
We applied the same procedural tests described in Shackelford et al.22 but modified them for single-grains of feldspar from sample LCC1 (as this sample contained slightly more feldspar grains than the other two) in line with Roberts76 and Rhodes77 protocols (Supplementary Table 14): 1) a preheat plateau test; 2) fading tests; 3) bleaching tests; and 4) dose recovery tests. Due to the small amount of grains in the 180–212 μm size fraction, we saved this for the De estimation and instead used the smaller 90–180 μm size fraction (and corresponding 200 μm single-grain discs) for all the procedural tests using the following preheat and IR stimulation combinations: 1) 250 and 225 °C (pIR-IRSL50,225)67,78; 2) 280 and 250 °C (pIR-IRSL50,250)79; 3) 300 and 270 °C (pIR-IRSL50,270)79; 4) 320 and 290 °C (pIR-IRSL50,290)80,81; and as the expected De is >450 Gy, we also tested 5) 320 and 200/290 °C (pIR-IRSL200.290)82. As many of the discs had very few feldspar decays, we used 4 single grains discs with a total of 16 grains and recycled these grains for all the tests. This is not ideal, and the use of fresh grains would have been preferred but the low feldspar yield meant that we had to prioritise the remaining sample for the actual measurements. All tests mostly followed the procedures outlined in Shackelford et al.,22 with the following differences:
Preheat plateau and dose recovery tests—the different preheat/IR laser stimulation combination was applied to each SG disc and to a different number of grains depending on how many grains luminesced on each disc. We then added a surrogate dose of 20 Gy to try and recovered this known dose from these discs.
Bleaching tests—the same 4 discs had a dose of 20 Gy applied and were bleached in a solar simulator and measured using the same preheat/IR laser stimulation combinations.
Following the protocols of Rhodes77 for testing anomalous fading in SG of feldspars, we employed 1) individual single-grain fading using the 4 discs for multiple delay times; 2) multiple grain measurements by using the SG discs as single-aliquots; and 3) the use of a standard fading value assessment by the degree of saturation for an infinite aged sample derived from the weathered granite pebbles found in the deposit and analysed using small single-aliquots.
The tests revealed that the flattest plateau was provided by the pIR-IRSL50,270, pIR-IRSL50,290 and pIR-IRSL200,290 signals (Supplementary Fig. 10c), while the pIR-IRSL50,270 signal provided the best recovery of the surrogate dose (with a dose recovery ratio of 0.995) and lowest residual values after bleaching (<10 Gy) (although calculated, these residual doses were not subtracted from the De) (Supplementary Fig. 10e). The pIR-IRSL50,290 and pIR-IRSL200,290 signals produced the largest residuals doses, which raises concerns over signal overestimation in this cave environment where there is a strong likelihood for partial bleaching. The fading tests from the single aliquot tests were much lower than from the single-grain tests, which revealed a range of fading from the highest IR50 to the lowest pIR-IRSL50,270, pIR-IRSL50,290 and pIR-IRSL200,290 signals (Supplementary Fig. 10d). We also observed a variation in fading rates among the single-grains (ranging from negative values to higher values that would not allow for any natural signal, with an average over the 16 grains of 2.3% per decade), but this was independent of the grains’ sensitivity. When using the pIR-IRSL50,270 signal on the single-aliquot discs, this g value was reduced to an average of 1.7% per decade. We decided to use a mean fading rate of 2.0 ± 0.2% per decade as a mid-point before the two techniques. Surprisingly the pIR-IRSL200,290 signal displayed the same amount of fading as seen in the pIR-IRSL50,270 and pIR-IRSL50,290 signals, indicating no apparent advantage in a higher initial temperature for IR stimulation in these samples.
The weathered granitic cobble provides the closest representation of the provenance of the feldspar grains from LCC1 and LCC2. Following the procedures of Brown et al.83, we used 12 very small single-aliquots (as the signal was too insensitive to use single-grains) and added large doses of 200 and 400 Gy to the natural signal (N + 200 Gy and N + 400 Gy) for eight discs and zero dose to the final four discs. All discs were measured using the ph/stimulation temperature combinations described above (Supplementary Fig. 10f). In all the discs, the IR50 signal grows with dose as does the pIR-IRSL50,225 signal to a lesser degree, but the pIR-IRSL50,290 and pIR-IRSL200,290 signals change by only a small amount. This indicates that the field saturation is close to the laboratory saturation using these signals. However, to be conservative we used a fading rate of 2.0% per decade. We used the fading correction method of Huntley and Lamothe84, which provides an estimation of the fading for small fading rates although it is designed for the linear portion of the growth curve.
As these feldspars contain very large De values close to the point of saturation, we conducted saturation tests on the same weathered cobble mentioned above83. We first ran the sample as a normal pIR-IRSL50,270 to observe the dose response of a saturated sample to ensure that the fitting procedure could accommodate these high dosing values.
Comments on the luminescence dating of the breccia
The feldspars had low sensitivities yielding very low acceptance rates; in all over 8,300 grains were processed with only 96 accepted grains (1.16% acceptance rate). The 180–212 size fraction was chosen for single-grain analyses as this was the largest size fraction available; the 90–125 size fraction yielded negligible feldspar grains. Rejections were based on the protocol of Jacobs et al.85 (see Supplementary Table 15). The grains were tested using XRD to verify that they were in fact K-rich feldspar grains, and the results indicated that they contained slightly lower than expected K contents (between 10.9 and 12.5%). Most of the grains had no decay whatsoever. These results were challenging considering the small amounts of sample yield meant that we were unable to get the number of accepted grains to a statistically meaningful number before running out of sample (LCC1- 48 grains, LCC2 - 25 grains and LCC3 - 23 grains). However, the value of the single-grain approach is that we can isolate individual dose populations rather than an average of many populations that result in a maximum age. Thus, the age estimate derived from the single-grain method (even with a small number of grains) is much closer to the true burial age of the sediments than a multiple-grain, single-aliquot approach.
The sedimentological and microsedimentological analyses provide clues as to the origins of the feldspar grains. The thin sections reveal a very low percentage of feldspar grains in the matrix, and this was confirmed by an analysis of the breccia itself, which contains minimal granitic pebbles. However, the few granitic pebbles found were highly weathered and could be the extra-karstic source for the K feldspar grains found in the samples. This also explains the low luminescence sensitivity of the grains. As for the bleaching potential of the grains - an extra-karstic origin bodes well for bleaching, but this depends on when the pebbles were weathered and released the K feldspar grains into the matrix. If weathered in situ, the chances for bleaching are reduced. This, combined with a rapid flooding event in a karst environment, is not the best scenario for bleaching grains. A single-grain approach in this situation is well justified to identify the grains that are the most bleached, however there is a chance that none of the grains have been bleached. In this situation even the apparently well bleached grains can still be overestimating the burial age, meaning that all the grains are effectively maximum ages. But when taken in the context of the relationship between the sediments and fossils, it is clear that the deposition of the sediments is the last event to occur as the flood waters would have gathered the fossils from the landscape (or incorporated already existing fossils from within the karst environment), resulting in the sediment ages being the youngest—even if they are maximum ages. The age of the sediments does not impact on the age of the fossils, which are all consistently older and had all accumulated by at least 104 kyr (the age of the overlying flowstone).
The striking difference between the environmental dose rate of the LCC1 (3.6 Gy/kyr) and LCC2 (5.0 Gy/kyr) in the same breccia unit can be explained by the heterogeneous nature of the deposit. The inverse grading suggests a rapid single karstic flood event of increasing energy. The flood waters deposited the arenitic silty clays before depositing the clasts in a coarsening, upwards sequence. At the point of LCC1, the clasts:matrix ratio was ~50% and was dominated by micritic and spartic limestone clasts; this increased to ~80% at LCC2 and was dominated by the granitic, quartzite and vein quartz pebbles derived from the underlying geology within a radius of ~20 km from the cave. This large difference in clast percentage and composition is enough to explain the difference in environmental dose rates. However, to make sure the values were indeed accurate we applied high resolution gamma spectrometry to both blocks. This produced a coeval result for LCC1 and a slightly higher dose rate for LCC2 (see Supplementary Table 3).
We used the high-resolution gamma spectrometry data from samples LCC1 and LCC2 to further investigate the differences in dosimetry and to test whether the deposit is in secular equilibrium. High resolution gamma spectrometry of the cave sediments is particularly useful as it provides information on the entire 238U and 232Th decay chains; therefore, the concentrations of the daughter as well as the parent nuclides can be explored. In this sedimentary environment, three potential disequilibrium states have been identified: 1) in the 238U chain a deficiency of 16% in 226Ra compared to 238U; 2) a 210Pb a deficiency of between 17 and 22% compared to 226Ra; and 3) in the 232Th chain, a small excess of 7% in 228Th compared to 228Ra. This disequilibrium is more pronounced in sample LCC2 than displayed in the sediments around LCC1.This is another example of the differences between these areas, which must again be attributed to the difference in clasts and composition and the capacity of the more clast-supported sediments in LCC2 to allow water seepage, the leaching of the more mobile radionuclides such as uranium and for radon loss. Thorium is thought to be immobile in most sediments86, and the short half-lives (t) of the daughter nuclides (228Ra = 5.7 yrs and 228Th = 1.91 yrs) and 210Pb (22 years) means that this effect of excesses in these radionuclides is negligible. The leaching of uranium appears to be more of a problem in LCC2 than LCC1, but a deficiency of 16% would only have a small effect on the total dose rate and has been incorporated into the error estimate for that sample. Both samples display a loss of radon as represented by a 210Pb deficiency compared to 226Ra, but the loss is 5.45% greater in LCC2. This can also be attributed to the presence of larger clasts that allow radon loss through the more matrix supported unit. However, radon loss does not explain why LCC2 has a much higher dose rate as the greater loss of radon in this sample should instead cause a decrease in dose rate. The limestone clasts could also be the source of the disequilibrium, which are more abundant in LCC2. As the mineralogical assemblage of the clay fraction does not vary between samples, the variation in 226Ra deficiency could reflect the proportion of limestone clasts in the sedimentary layers. Despite all of these differences, the main largest difference in the environmental dose rate between the samples is an almost doubling of 40K in LCC2. This could be derived from the higher potassium feldspar content from the weathered granitic cobbles.
The environmental dose rate of the breccia (3.6–5.0 Gy/kyr) is significantly higher than the lower silty unit at 2.7 Gy/kyr. Thus, the resulting breccia De values were very high at between 400 and 2000 Gy with D0 values of between 600 and 1000 Gy. This meant that some grains were close to the point of saturation (~1000–1200 Gy) and pushed the limits of feldspar dose saturation. This made the rejection criteria of utmost importance to ensure that the saturated grains were not included in the accepted grains. The feldspars obtained from the weathered cobble provides the best test of the saturation characteristics of these samples, as they have never been bleached so they should display an infinite age. The initial fading test using these grains displayed grains that saturate ~1500–2000 Gy with D0 ~600–1000 Gy. This is within the limits of our De estimation.
Due to the problems associated with uranium leaching in cave environments we decided to use the environmental dose rates derived from the high-resolution gamma spectrometry as a more conservative approach. Using these dose rates, the three blocks produced age estimates that are consistent with their stratigraphic location and within their error margins (within 1 σ). The two breccia age estimates (LCC1 143 ± 24 and LCC2 133 ± 19 kyr) are statistically indistinguishable from each other despite having a large difference in dose rates (3.6 and 5.0 Gy/kyr, respectively). This suggests that the breccia matrix had indeed been deposited rapidly within one unit, as suggested by the sedimentological analyses. The underlying silty unit (LCC3 248 ± 31 kyr) with minimal clasts had a much lower dose rate and much lower feldspar grain acceptance rate (0.2 %), indicating a different composition and/or different depositional circumstances. All three samples contained a wide range of De values with overdispersion values of between 23–38%. This justified the use of the MAM, which has identified the grains that were the most bleached prior to burial inside Tam Ngu Hao cave.
Uranium series dating of flowstone
U-series dating of the overlying flowstone at Tam Ngu Hao 2 provides a minimum age for the deposition of the breccia and associated fossils. Four separate sub-samples were drilled from the fresh cross-section of a hand specimen of the in situ flowstone using a hand-drill. Calcite was sampled from the in situ flowstone using a hammer and chisel. The powdered sub-samples were subjected to chemical treatment and isotopic measurements by mass spectrometry87. U-series dating of the speleothem samples was conducted in the Radiogenic Isotope Facility (The University of Queensland) using a Nu Plasma multi-collector inductively coupled mass spectrometer (MC-ICP-MS). Analytical procedures followed previous publications for MC-ICP-MS87,88,89. 230Th/234U ages were calculated using Isoplot EX 3.7590 and half-lives of 75,690 years (230Th) and 245,250 years (234U)91.
Comments on the uranium series dating of the flowstone
The overlying flowstone is composed of poor-quality calcite and has a high detrital component in all four sub-samples, as reflected by the high levels of 232Th concentrations and very low 230Th/232Th activity ratios (0.84 to 1.0) that afforded imprecise and unreliable age results. This flowstone is at least younger than 153 ± 1 kyr, which is the youngest uncorrected age among all four sub-samples (i.e., the maximum age of the sub-sample). The non-radiogenic 230Th correction using the standard Bulk-Earth 230Th/232Th activity value of 0.825 with an assumed uncertainty of 50% for non-radiogenic 230Th correction has resulted in very large error magnifications, with one of the four sub-samples returning a negative age value, pointing clearly to over-correction of the non-radiogenic 230Th. A better estimate of the most reliable correction is based on the assumption that the real detrital 230Th/232Th activity ratio should be lower than the bulk-Earth value of 0.825. In order to obtain a better estimate, we plot the measured 234U/232Th activity ratios against the measured 230Th/232Th activity ratios, which defines a best-fit line with an intercept value of 0.5 on the 230Th/232Th axis. In other words, this intercept represents the common initial (or detrital) 230Th/232Th activity ratio of the four sub-samples. Thus, a new correction scheme using a non-radiogenic 230Th/232Th activity value of 0.5 is more appropriate. Based on this new scheme, the four sub-samples give indistinguishable corrected ages with a weighted mean of 104 ± 27 kyr (See Supplementary Table 4 for details). When trying to establish the age of the underlying breccia, this result as a standalone age estimate is not particularly useful, but as part of a chronological section it does provide a ‘minimum’ age estimate for the entire stratigraphic sequence of flowstone, breccia and underlying silty unit and has thus been used in the Bayesian model.
Coupled uranium series and electron spin resonance (US-ESR)
Three bovid teeth (TNH2-10/CC10, TNH2-11/CC11, TNH2-12/CC12) recovered from the upper fossil-bearing breccia (LU2) were used for direct dating by coupled US-ESR following the protocol of Joannes-Boyau et al.92,93,94 (Fig. 1b). All three teeth were first sectioned in half using a benchtop high precision diamond saw then polished to a 50 μm smoothness to expose a flat surface of dentine and enamel for 238U concentration screening using an ESI NW213 and ICPMS quadrupole Agilent 7700 for concentration. A small fragment of dentine and enamel of each faunal tooth was then removed using a 300 μm thick diamond blade attached to a hand-held rotary saw for U-series analyses using a LA-MC-ICPMS Thermo Neptune plus coupled to an ESI NW193 laser ablation unit (Supplementary Fig. 11). Isotopic ratios and concentrations were obtained by LA-MC-ICPMS and quadrupole ICPMS analyses, respectively. An average value was calculated for each dental tissue and used for the US-ESR model. Baseline and drift were corrected using a NIST 612 glass disc, while a fossil hippopotamus tooth of known U-series concentration was used to correct 234U/238U and 230U/238U ratios and assess the accuracy of measurements. Another enamel fragment from each tooth was used for ESR measurements. ESR dating was performed on a Freiberg MS5000 X-band spectrometer at 1 G modulation amplitude, 2 mW power, 100 G sweep, and 100KHz modulation frequency, coupled to a Freiberg X-ray irradiation chamber, which contains a Varian VF50 x-ray gun at a voltage of 40KV and 0.5 mA current95,96. Fitting procedures were carried out with the MCDoseE 2.0 software that uses a Bayesian framework approach where the solution is a full probability distribution on the dose equivalent97.
The CC10, CC11 and CC12 enamel fragments removed from each sample and used for the ESR measurements were directly in contact with the dentine on one side and directly in contact with the sediment on the other side (no cement). The outer surface of the enamel (in contact with the surrounding sediment) and the dentine directly attached to it were removed using a diamond blade rotary tool. Simultaneously, 100 μm on each side was removed to avoid alpha particle contribution. Each tooth fragment was then cut in three separate pieces (A, B and C), with A (50 Gy) and B (200 Gy) to be pre-irradiated with one single gamma dose prior to the x-ray irradiation and C irradiated with x-ray solely. Fragments were mounted onto a teflon sample holder, allowing the fragment to be exposed directly to the x-ray source behind a 200 μm aluminium cover shielding. To estimate the ESR equivalent dose (De), each fragment was irradiated seven times, following exponentially increasing irradiation times (i.e., 90 s, 390 s, 975 s, 1891s, 3604 s, 7380 s and 12382 s with an average dose rate for CC10, CC11 and CC12 of 0.231 Gy/s, 0.203 Gy/s and 0.249 Gy/s, respectively). The x-ray emission received by the bovid teeth was calibrated using added known gamma irradiation doses on fragments A and B performed at the Australia’s Nuclear Science and Technology Organisation (ANSTO). During each irradiation step, the output of the x-ray gun was recorded to allow an accurate determination of the dose received by the sample at each step. The dose response curves (DRCs) were obtained by averaging the peak-to-peak T1-B2 ESR intensities recorded for each irradiation dose over 180° measurements (20o step) and merged into a single spectrum98. Isotropic components and baseline corrections were applied uniformly across the measured spectra94.
The direct dating of TNH2-1 was attempted but to minimise damages to the valuable sample, the superficial layer of residual dentine at the root vestige was used. Unfortunately, analyses have shown a high degree of diagenesis to the micro sample that completely overshadowed any meaningful interpretation of an age for the fossil.
Comments on coupled uranium series and electron spin resonance (US-ESR)
A non-orientated components (NOCORs) of the ESR signal of 16%, 14 and 8% for TNH2-10/CC10, TNH2-11/CC11 and TNH2-12/CC12, respectively, was extracted using the Joannes-Boyau94 method from the signal. The final De values were obtained by fitting a single saturating exponential (SSE) through the ESR intensities and by selecting the appropriate maximum irradiation dose (Dmax) in order to avoid dose estimation inaccuracy99. All errors were calculated with a 2-sigma interval. Sediments surrounding the teeth were collected and analysed in solution by ICPMS after an acid (1:3 Nitric and HCL) digestion method. The external gamma dose rate was calculated using the sediment content measured by ICPMS and assuming a full 4π geometry. The total dose rates for TNH2-10/CC10, TNH2-11/CC11 and TNH2-12/CC12 were calculated at 1482 ± 224, 1253 ± 192 and 1187 ± 208, giving US-ESR ages of 164 ± 24 kyr, 149 ± 22 kyr and 140 ± 23 kyr, respectively, using a Monte Carlo approach100 (Supplementary Table 2) and assuming equilibrium for the rest of the decay chain. However, the uranium diffusion fits the open-system model with accumulation of uranium at the enamel dentine junction and in cracks as well as presence of leaching of uranium and enrichment of thorium 232. For sample TNH2-10/CC10, the 230Th/234U ratio in the enamel had to be assumed (see Supplementary Table 2(*)) because of leaching and/or sediment enrichment (measured 230Th/234U ratio >1 and concentration of U is low while thorium is high). Unfortunately, in order to model the age using the Monte Carlo calculation from Shao et al.100, we used the same 230Th/234U ratio to that of the dentine for the enamel, introducing a sizable assumption into the age calculation of this particular sample. Under these conditions, the combined age estimate places the sequence slightly older than 150kyr. TNH2-10/CC10 remains slightly older, but within error of TNH2-11/CC11 and TNH2-12/CC12, and therefore statistically indistinguishable. Furthermore, the dose equivalent (De) of TNH2-10/CC10 was calculated to be 1.3 and 1.5 times greater than for TNH2-11/CC11 and TNH2-12/CC12, respectively (Supplementary Table 2). Additionally, the NOCORs concentration for TNH2-12/CC12 might have been underestimated due to an unusually poor angular response of the fragment. A similar NOCOR content as for TNH2-10/CC10 or TNH2-11/CC11 would increase the De by ~8%, which would bring the age closer to TNH2-11/CC11. The spatial distribution of the U-series results of each tooth gives a better understanding of the diffusion process within the dental tissues (see Supplementary Fig. 12a–c). Apart from punctual intrusion of sediments in cracks and other dental defects (Supplementary Fig. 12c), the distribution is characteristic of a diffusion pathway with uptake from pulp cavity into the dentine or to a lesser extent from surrounding sediments to the outer layer of the enamel in contact with the sediments. The age and concentration gradient observed with the distance moving away from the uptake origin is not reflected in the U-series ratio measured. Thus, potential leaching and/or late enrichment may have occurred but would be marginal with regards to the age calculation. This diffusion pattern reinforces the U-series age results and gives an average age estimate of 189 ± 9 kyr, 132 ± 13 kyr and 124 ± 16 kyr (2-sigma) for TNH2-10/CC10, TNH2-11/CC11 and TNH2-12/CC12, respectively. The p-value (diffusion function in dental tissues of uranium) in all three teeth is approaching −1 or in other words, equivalent to an early uptake of the isotopes into the teeth. This in turn explains why both U-series and US-ESR dating results are within error of each other. In summary, the US-ESR results of the faunal teeth provide a weighted mean age of 151+/− 37 kyr for the human remains. At last, while the fossil teeth were unearthed at a depth of 20 cm from the surface, the structure of the breccia indicates that a large part had eroded away in the recent time. Therefore, the external dose rate was modelled assuming a full 30 cm sphere of breccia surrounding each fauna sample. If we model the external dose rate to the current burial configuration, the external dose rate would amount to 699+/−121mGy/kyr. Because of the significant role of the external component to the total dose rate, the age estimates would be shifted to 190+/−28kyr, 177+/−26kyr and 168+/−27kyr for CC10, CC11 and CC12 respectively.
Modelling of the breccia unit and associated fossils
To evaluate the uncertainties of the integrated dating approach to the site (Supplementary Tables 1–4), Bayesian modelling was performed on all independent age estimates using the OxCal (version 4.2) software101 available at https://c14.arch.ox.ac.uk/oxcal.html (Supplementary Fig. 3). The analyses incorporated the probability distributions of individual ages, constraints imposed by stratigraphic relationships and the reported minimum or maximum nature of some of the individual age estimates. Each individual age was included as a Gaussian distribution (with mean and s.d. defined by the age estimate and their associated uncertainties), and the resulting age ranges for each unit are presented at 1 σ.
No attempt was made to remove identified outliers. This is because we do not know the underlying’true’ age depth model, and we are using several different dating methods so it is difficult to specify the criterion to identify true outliers. Rather than this approach, we have explicitly specified minimum and maximum ages where appropriate to do so in keeping with the nature of the dating methods and the quality of the results. We believe this is a superior method compared to outlier analysis in this context, as it avoids unnecessary bias (e.g., in the choice of criterion) and represents a more conservative approach.
Comments on modelling of the breccia unit and associated fossils
The age estimates are coeval and the uncertainties are relatively small. As such, the identified boundary ages are not sensitive to removal of individual dates or to changes in, for example, the model calculation resolution. None of the changes we made to the model set-up produced appreciable differences in the age model results. The age of the breccia at Tam Ngu Hao 2 was conservatively estimated as the boundary between the overlying flowstone unit (104 ± 27 kyr) and the age estimates of the breccia and fossils from within the breccia (131 ± 15 kyr) and the boundary between the breccia and underlying silt unit (164 ± 17 kyr), incorporating all of the constraints described above and the resulting age estimates (Supplementary Tables 1–4). The final modelled ages are presented in Supplementary Fig. 3 and the script presented in Supplementary Fig. 13. The age estimates from the breccia, derived from both US-ESR dating of teeth and pIR-IRSL dating of breccia matrix, are coeval within error margins despite constraining two different events, i.e., the death of the fauna and the deposition of the breccia unit, respectively. This indicates that the timing between death and final burial within the cave was very short, and that the breccia was deposited rapidly as one unit.
Detailed morphological analysis of the tooth
Description of TNH2-1
TNH2-1 is an isolated mandibular left permanent molar crown germ with the root growth just initiated and reaching ~1.8 mm below the crown (Fig. 2a–f). The enamel is well-preserved, showing a shiny beige patina with whiter spots. There is a slight enamel hypoplasia toward the cervix and minute pits at mid-crown height on the buccal and mesial aspects, but no carious lesion. The dentine is dark brown on the external surface with some locally altered areas showing that the underlying dentine is yellower. The occlusal outline is sub-pentagonal. The absence of occlusal wear (stage 1102) and of interproximal mesial and distal facets indicates that the tooth was still unerupted at the time of death. There are five main cusps (protoconid>entoconid≥hypoconid>metaconid>hypoconulid) connecting in a + groove pattern in the middle of the occlusal basin, as well as a tuberculum sextum (C6) located on the hypoconulid distal marginal crest (Fig. 3). There is a prominent shoulder on the mesial crest of the hypoconid that manifests as a small tubercle at the enamel surface. There is a high and continuous middle mid-trigonid crest (with a slight depression centrally) and an interrupted distal trigonid crest with a buccal segment initiating on the distal ridge of the protoconid and a lingual segment originating on the distal ridge of the metaconid (type A103). This trigonid crest pattern corresponds to a type 8 pattern of Martinez de Pinillos and collaborators classification103, with a continuous mid-trigonid crest and a discontinuous distal trigonid crest arising from the distal segments. There are also shorter crests set distally to the distal trigonid crest and larger crests running from the talonid cusps down toward the centre of the occlusal basin. The anterior fovea is narrow, buccolingually extended and deep (type 4 according to ASUDAS104,105). There is no protostylid (type 0 according to ASUDAS104,105) although a faint buccal shelf is detected along the buccal face at the EDJ (Fig. 3b). At the EDJ, it can be observed that the mesial dentine horns are more centrally placed and more tilted toward the centre of the occlusal basin than the distal ones. In inferior view, five pulp horns are discernible despite the immature stage of the pulp chamber.
The overall pentagonal crown shape with subparallel buccal and lingual walls, the presence of a complete mid-trigonid crest, the well-expressed hypoconulid and C6, as well as the mesiodistally elongated diameter (see Figs. 2 and 3; Supplementary Fig. 2; Supplementary Tables 10 and 11) suggest that it more likely represents a first or second molar rather than a third molar. Statistical analyses performed on the EDJ shape (see Supplementary Table 16) classify TNH2-1 as an M2, but its marked resemblance with the M1 of the Xiahe mandible (as attested by the close position of both teeth in the GM analyses of the EDJ) and obvious difference with the M2 of the latter that shows an unusual occlusal morphology (with a marked buccolingual extension of the occlusal basin associated to the presence of a supernumerary root below; see ref. 15) cast doubts about its metameric position (see Supplementary Fig. 5). The fact that the M1 and the M2 of the Xiahe specimens are both classified either as M1 (in the semilandmark analyses; Supplementary Table 16) or as M2 (in the DSM analyses; Supplementary Table 16) may also indicate a particularity of Denisovan molars. Indeed, while the unsecure attribution of the M2 is not surprising considering the above mentioned unusual EDJ shape, the M1 exhibits no anomaly and should be classified as a M1 in both analyses. As indicated by the difficulty to identify the Denisova 4 and 8 molars as M2s or M3s, this ambiguous result regarding the Xiahe molars may imply that Denisovan molar metameric variation differs from that of the groups included here as reference, preventing us from unambiguously attributing TNH2-1 to a M1 or to a M2 if it belongs to the latter group.
The TNH2-1 specimen was scanned using the X-ray microfocus instrument (X-µCT) diondo d3 at the Max Planck Institute for Evolutionary Anthropology, Leipzig, Germany. Acquisitions were performed according to the following parameters: 130 kV, 70 µA, 0.5 mm brass filter, 2970 images taken over 360° (~0.12° of angular step) with an averaging of 2 (frame averaging), integration time of 1000 ms. The final volumes were reconstructed with a voxel size of 9.14 µm. The microtomographic acquisitions of the comparative fossil and extant hominid specimens were performed using various equipments including X-µCT and synchrotron radiation (SRX-µCT) and reconstructed with voxel sizes ranging from 10.25 to 57.50 µm.
A semi-automatic threshold-based segmentation was carried out in Avizo 8.0 (FEI Visualization Sciences Group) following the half-maximum height method (HMH106) and the region of interest thresholding protocol (ROI-Tb107), taking repeated measurements on different slices of the virtual stack108. A volumetric reconstruction was then generated for each specimen.
The mesiodistal and buccolingual tooth crown diameters of TNH2-1 were measured on the original specimen with Mitutoyo Digimatic calipers (to the nearest 0.1 mm) and then on the virtual surface generated after segmentation of the microtomographic record. These measurements were compared with the tooth crown diameters of H. erectus s.l. (HE), H. antecessor (HA), European Middle Pleistocene Homo (EMPH), Asian Middle Pleistocene Homo (AMPH), Neanderthals (NEA), Upper Palaeolithic H. sapiens (UPMH), and Holocene humans (HH) (see Supplementary Tables 9, 10). Adjusted Z-score analyses109,110 were performed on the mesiodistal and buccolingual diameters of TNH2-1 in comparison with the comparative specimens/samples. This statistical method allows the comparison of unbalanced and small samples, which is often the case when dealing with the fossil record, using the Student’s t inverse distribution following the formula: [(x-m)/(s*sqrt(1 + 1/n)]/(Student.t.inverse(0.05;n-1)), where x is the value of the variable; m is the mean of the same variable for a comparative sample; n is the size of the comparative sample; and s is the standard deviation of the comparative sample (Supplementary Table 11).
3D crown tissue proportions
Three variables describing tooth crown tissue proportions were digitally measured on TNH2-1: the percent of the crown volume that is dentine and pulp (Vcdp/Vc; %), the average enamel thickness (3D AET; mm) and the scale-free 3D relative enamel thickness (3D RET)111,112,113. Intra- and interobserver accuracy tests of the measures run by two observers provided differences <5%. Adjusted Z-score analyses109,110 were performed on the tooth crown tissue proportion parameters for TNH2-1 in comparison with the comparative specimens/samples.
Geometric morphometric analyses of the enamel-dentine junction (EDJ) shape
We used a diffeomorphic surface matching (DSM) approach to analyse the EDJ conformation. This method constructs shape atlases using mathematical currents (functions to analyse manifolds), where topology of the template is preserved and deformation parameters are optimised independently of the shape parameters114,115,116). We used the Deformetrica v. 4.3 software (https://www.deformetrica.org) to generate a global mean shape with a set of diffeomorphisms relating the global mean shape to each individual and the output (control points and deformation momenta) to perform the statistical analyses, and explore the EDJ shape variation and classify the data. This approach has already been used to study the EDJ shape of fossil hominins and proved to be a reliable method to discriminate between taxa117,118. Fitting deformation-based models were applied to the complete EDJ decimated to 50,000 polygons and aligned by Procrustes superimposition. Smooth and invertible deformations combined with a metric of currents that defines a distance between EDJ surfaces allowed us to quantify the degree of shape variation between the investigated specimens. The global mean shape and the deformations functions were then used to classify the data. We also compared the results of the DSM analyses with those obtained with a classic geometric morphometric method based on landmarks and semi-landmarks placed along the EDJ occlusal and cervical margins. More precisely, four anatomical landmarks were placed on the tip of the dentine horn of four primary cusps (protoconid, metaconid, entoconid, and hypoconid) and a first set of semi-landmarks was positioned along the top of the marginal ridge connecting the dentine horns (beginning at the top of the protoconid and moving in a lingual direction), while a second set of semi-landmarks was placed along the cervix starting below the protoconid dentine horn (specifically, the mesio-buccal corner of the cervix) and moving in a mesial direction39. Where small parts of the cervix were missing, its location was estimated. In most cases the cervix landmarks were placed on a surface model of the whole dentine crown as this is most appropriate and facilitates placing landmarks on specimens in which missing enamel impacts the completeness of an EDJ surface. Geometrically corresponding semilandmarks119 were derived in Mathematica (Wolfram Inc.) by using a software routine120,121 following the measurement protocol detailed in Skinner et al.122,123. A smooth curve was interpolated using a cubic spline function. The cubic spline was fitted by starting at the first landmark and moving in a lingual direction to the last point. The interpolated curves were then resampled to achieve identical point counts among specimens. The semi-landmarks of the EDJ marginal ridge were then projected onto the curve, dividing the curve into four sections (protoconid to metaconid: 12 landmarks; metaconid to entoconid: 12 landmarks; entoconid to hypoconid: 24 landmarks; hypoconid to protoconid: 12 landmarks). For the semi-landmarks at the cervix, 30 equally spaced landmarks were generated along the cervix curve.
For both geometric morphometric approaches, we then performed generalised Procrustes analyses, followed by principal component analyses (PCA). We investigated the structure and group separation along the PC scores, checking that the groups already pre-exist in the PCA (Supplementary Fig. 7). Both DSM and landmark-based approaches show a substantial degree of separation between taxa along the first three PC axes (Supplementary Fig. 7). We computed canonical variate analyses (CVA) and between-group principal component analyses (bgPCA). The following three groups were used in both CVA and bgPCA: H. erectus s.l. (HE), European Middle Pleistocene Homo and Neanderthals (EMPH-NEA), Pleistocene and Holocene H. sapiens (MH). TNH2-1 and the two molars (M1 and M2) of the Xiahe mandible were then projected a posteriori in the CVA and bgPCA. The CVA was conducted based on the first few principal components explaining ~90% of the total variance124 (18 in the landmark-based and 24 in the deformation-based analyses; Fig. 5a, Supplementary Fig. 7). We also performed cross-validated canonical variates analyses (CV CVA) still based on the first few principal components explaining ~90% of the total variance for both DSM and landmark-based data (Supplementary Fig. 7). The CV CVA was done first to check the probability that the TNH2-1 specimen represents an M1 or an M2 (Supplementary Table 16) and then with the same groups for the bgPCA to assess the taxonomic prediction (Supplementary Table 17). The bgPCA was computed based on the deformation moments (Fig. 5b) and Procrustes residuals (Supplementary Fig. 7). The DSM and landmark analyses gave similar results for the both CVA and bgPCA, although the DSM method better discriminates the groups (Fig. 5b, Supplementary Fig. 7). The fact that two different GM approaches (DSM and landmarks) reproduce comparable group discrimination and distribution when using either CVA or bgPCA, that are computed with different input data (a selected set of PC scores and the moments/Procrustes residuals, respectively), suggests that the results of the geometric morphometric analyses are robust. We also followed the recommendations of Cardini and Polly regarding the validity of bgPCA125 by computing the cross-validated bgPCA (CV bgPCA; Supplementary Fig. 7) and comparing it with the bgPCA (Fig. 5b, Supplementary Fig. 7h), showing that both display the same degree of group discrimination. Results of the CV CVA (Supplementary Table 17) and CV bgPCA show a high level of correct classification (HE: 94.1%; EMPH-NEA: 98.0%; MH: 88.2% for the bgPCA based on DSM with three groups). In order to test further that groups separation in not artificial, we also computed the bgPCA with five groups instead of three (including H. erectus, and separating Middle Pleistocene and Late Pleistocene Neanderthals, as well as Pleistocene modern humans and Holocene humans; Supplementary Fig. 7). These analyses show nearly identical taxonomic distinctions than in the bgPCA based on three groups (H. erectus, Neanderthals and modern humans; Fig. 5b, Supplementary Fig. 7), indicating that groups separation reflects the biological reality. Altogether, the PCA and bgPCA, CV bgPCA and CVA analyses based on landmarks and DSM are consistent with each other and confirm that the groups observed in the bgPCA are not spurious126. The analyses were performed using the packages ade4 v.1.7-6127 and Morpho v. 2.7128 for R v.3.4129. Allometry was tested in the semi-landmark analyses using multiple regression130 in which the explanatory variable is the centroid size and the dependent variables are the PC and bgPC scores. In all PCA and bgPCA, the first two components show no allometry (p-value > 0.05). The differences between specimens thus represent shape-variation.
Ancient protein analysis
Enamel protein extraction followed protocols detailed elsewhere34. In short, small enamel samples were demineralised in either hydrochloric acid (HCl) or trifluoroacetic acid (TFA), cleaned up on C18 stagetips and subsequently analysed using nanoLC-MS/MS without protease digestion or cysteine reduction and alkylation.
The proteome of the TNH2-1 enamel was analysed with a previously published workflow34. The sample was processed in a clean lab suitable for ancient DNA and protein analysis. The enamel was mechanically cleaned, and two small samples (12 and 13 mg) were removed and powdered for protein extraction. For demineralisation, the enamel powders were suspended in either 1.5 M (5.5% w/w) HCl or 0.88 M (10% w/w) TFA and incubated at room temperature overnight. Peptides were extracted from the supernatant and desalted by solid-phase-extraction using C18 Stagetips131. Laboratory blanks were prepared using the same procedure. The peptides were vacuum-dried, reconstituted in 0.1% TFA 5% ACN and quantified using a Nanodrop spectrophotometer at 280 nm. Approximately 500 ng peptides were loaded on a 75 µm inner diameter, 15 cm length column home-packed with 1.9 µm Reprosil-Pur C18 beads (Dr. Maisch) with a laser-pulled silica emitter. The analytes were separated using an EASY-nLC 1200 (Thermo Scientific) and two different gradients using 0.1% TFA 99.9% water as solvent A and 0.1% TFA 80% ACN 19.9% water as solvent B at a flow rate of 350 nL/min. The shorter 45 min gradient increased from 8 to 15% B over 25 min, to 30% B over 15 min, and to 45% B over 5 min. The longer 90 min gradient increased from 8 to 20% B over 75 min, from 20 to 30% B over 10 min and from 30 to 45% B over 5 min. The LC was interfaced with an Orbitrap Q-Exactive HF-X (Thermo Scientific)132, acquiring full MS scans from 350 to 1400 m/z at 60,000 resolution at 200 m/z, 3e6 AGC target, and 45 ms max. Injection time (IT) was followed by 10 data-dependent MS2 scans with 1.3 m/z isolation width and HCD fragmentation at a normalised collision energy of 28 and measured at 45,000 resolution, 1e5 AGC target, 45 ms max. IT, and a first mass of 100 m/z. The raw files were analysed with Maxquant version 220.127.116.1133 searching against an in-house curated database containing protein sequences expected in the Hominidae enamel proteome35,36. Candidate peptides were generated by “unspecific” digestion and allowed for up to 3 of the following variable modifications: deamidation (NQ), hydroxyproline (P), phosphorylation (STY), oxidation (MW), dioxidation (W), kynurenine formation (W), and arginine-to-ornithine conversion (R), which were chosen based on a previously published open-search strategy134 using the “dependent peptides” search feature of Maxquant. The Maxquant search also included the approximately 3-centuries old enamel proteome from a human (Ø1952, male, Homo sapiens) that was previously prepared and analysed in an identical manner35, as well as numerous extraction and mass spectrometry blanks.
Extraction and mass spectrometry blanks contained no proteins, indicating clean extraction and instrument conditions during analyses. Subsequently, proteins represented by a single peptide and likely contaminants were removed from analyses. This left a small number of known enamel proteins for further phylogenetic and diagenetic analyses (Supplementary Table 7). Spectra overlapping amino acid positions with sequence differences between Neanderthals, Denisovans, the Xiahe Denisovan, and H. sapiens were inspected manually to determine a phylogenetic assignment. Here, spectra with incomplete fragmentation around sites of interest were excluded from consideration. No high-confidence spectra were identified, making it impossible to assign TNH2-1 to any of these three groups based on palaeoproteomic data. A similar inspection of phylogenetically informative sites among great apes indicates that TNH2-1 represents a hominin (Supplementary Fig. 14; Supplementary Table 8).
Protein modifications that were previously identified in early Pleistocene enamel34 were quantified by relative spectral counting. Therefore, the number of peptide-spectrum matches (PSMs) containing a certain PTM was divided by the total number of PSMs containing the respective amino acid(s) that can be modified. The sequence motif analysis of peptides containing a phosphorylated serine residue was done using the R-package “ggseqlogo”135. The R scripts for the PTM analyses and construction of Supplementary Fig. 4 are available in the supplementary data 1. Peptide fragment spectra covering sites relevant for phylogenetic placement were annotated using the “Interactive Peptide Spectral Annotator” webtool136 (Supplementary Fig. 14; Supplementary Data 1) and calibrated peak lists from Maxquant. Raw data and peptide identifications resulting from our MaxQuant analyses are available on ProteomeXchange137 (PXD018721).
Associated fauna from Tam Ngu Hao 2 cave
Thirty-eight identified teeth (one deciduous and 37 permanent) of suids and numerous small fragments display the morphological pattern of Sus with bunodont cusps and cuspids on molars and numerous accessory tubercles. Only 12 teeth (most premolars) out of 38 are complete, with the majority being fragmentary or broken. We did not see significant differences on teeth that would suggest the presence of several species. On two well-preserved m3s (particularly the complete TNH2-117) (Fig. 6j–k), the anterior cingulum is marked and the median accessory cuspids are well developed. It is also notable on one M3 (TNH2-125), with well-developed cingulum and median cusp (hyperconule) behind the first row like in Sus scrofa (versus Sus barbatus138). The dimensions taken on few teeth fall in ranges of Sus scrofa from the late Middle Pleistocene to Late Pleistocene Indochinese sites28,139,140,141, unlike Sus lydekkeri which was much larger25 (Supplementary Data 2).
Thirty-five permanent teeth of large bovids are massive with a relatively thick enamel (a feature that helps distinguish bovids from cervids of comparable size and among large-sized bovids, Bos from Bubalus, based on our own observations). Most of the teeth are fragmentary, and within the set of permanent teeth only three (one right p3, one left p2, and one lower right m3) provide systematics input. The p2 is small and massive like in Bos as opposed to elongated as in Bubalus (Fig. 6x, y). The valleys are also shallow like in Bos. The parastylid and the paraconid of the p3 are less developed in comparison with the posterior cuspids. The metaconid is oriented posteriorly. Dimensions of p2s and p3s fall within the size ranges of the modern Bos gaurus (Fig. 27 from ref. 142). On m3, we note a salient entostylid, which forms a deep notch with the hypoconulid. Even if morphological and morphometrical data are not directly comparable, the outline and the orientation of the hypoconulid on the m3 are closer to those of the Late Pleistocene Bos gaurus frontalis (Fig. S4c from ref. 143) (different nomenclatures are available for this taxon: Bos gaurus144; Bos frontalis145,146,147). Five fragmentary milk teeth and one complete left d3 are likely to be associated with this set of permanent teeth. The large bovid of TNH2 can be assigned to Bos sp., possibly B. cf. frontalis.
Bovids from TNH2 cave also include one small-sized caprine with three almost complete and three fragmentary isolated teeth. One fragmentary maxilla still covered by hard breccia sediment displays the left side with D4, M1, and M2 still in the bone (TNH2-94) (Fig. 6i). Another fragment preserves the right side with M2 as a germ (TNH2-95). All this material displays the archetypical pattern of the subfamily with rather smooth enamel (not so ridulated as in cervids) and styles and stylids that are more prominent than main cusps and cuspids. One lower molar shows an ectostylid not common in caprines to our knowledge, and observed on one specimen of the modern Naemorhedus goral from India (MNHN-specimen 1939–243). Dimensions of the three molars are compatible with the size ranges of a small-sized Naemorhedus species (Fig. 34 from ref. 142), the infraspecific identification of which remains impossible with the available remains (Supplementary Data 2).
Twenty-three teeth (19 permanent and 4 deciduous) exhibit a morphological pattern and dimensions similar to those of a large deer: ridulated enamel, large cusps and cuspids on molars, well-developed ectostylid and entostyle on lower and upper molars, respectively (Fig. 6u). Four well-preserved lower premolars, one fragmentary p2, two p3s and one p4 could belong to Rusa unicolor. The p4 is not fully molarized and shows a partial closure of the valley (formed by the metaconid and the paraconid) (Fig. 6s–t). Overall, dimensions of the teeth (Supplementary Data 2) are small and closer to those of the large cervid recovered at Coc Muoi (late Middle Pleistocene, Vietnam28) and to those of the Khok Sung site (Middle Pleistocene, Thailand142) rather than to those of the Tam Hay Marklot site (Late Pleistocene, Laos141).
A set of identifiable small teeth of Artiodactyla, most fragmentary, suggests the presence in the assemblage of small and medium-sized cervids (Fig. 6m–n, ab–ae). Among twenty-four teeth, one m3 and one m1/m2, one elongated lower p2 (parastylid straight, metaconid oriented posteriorly), and two p3/p4 all worn, one elongated d2 and two D4s, along with several P3/P4s have a morphology and dimensions consistent with those of Muntiacus (Supplementary Data 2). The identification at the species level, however, is impossible with the available material. Six teeth most likely belong to a medium-sized cervid, among which two worn and fragmentary molars, one incisor, one d4 (TNH2-196), one incomplete milk tooth, and one D2 (TNH2-32). It is morphologically and metrically close to the small-sized cervid from Tam Hay Marklot, tentatively identified as Rucervus eldii (Late Pleistocene, Laos141), and to that of Coc Muoi (late Middle Pleistocene, Vietnam28).
The rhinocerotid sample mostly includes fragments of isolated teeth. Nine permanent teeth (P/p and M/m) and three milk teeth are too fragmentary to allow for more precise identification than Rhinoceros sp. (TNH2-170, TNH2-177, and TNH2-179) or Rhinocerotina indet. (i.e. Rhinoceros or Dicerorhinus) (Fig. 6c–e, h). Nevertheless, morphology and dimensions of nine other specimens are more informative. Among them, two incomplete teeth have morphological features and dimensions fully compatible with Rhinoceros sondaicus: i) a left p3 (TNH2-188) with a short, thick and smooth labial cingulid and a shallow ectolophid groove, perfectly matching that of the jaw n°305c from Soember Waroe (Middle Pleistocene, Java; Fig. 13 from ref. 148) and the p3 CM1027 from Coc Muoi (late Middle Pleistocene, Vietnam28); and ii) a left d2 (TNH183) which is narrow with a bulbous paralophid and no anterolabial groove that falls in the range of the large R. sondaicus sample from Coc Muoi28. A small and fragmentary right D4 (TNH2-184) with a sigmoid protoloph and an anteriorly-constricted protocone documents Dicerorhinus sp., but its fragmentary condition precludes any assignment at the species level. One tapir (Tapirus sp.) completes perissodactyl taxonomic diversity at TNH2 cave, with the posterior lophid (hypolophid) of a fragmentary d4 (TNH2-178) that is too small to be assigned to Megatapirus (width: 19.5 mm instead of 22–23 mm in the latter taxon) and is instead compatible with both T. indicus indicus and T. i. intermedius25. Several enamel fragments, both thick and wrinkled, unambiguously point to the presence of a stegodon elephantiform (Stegodon sp.).
Small-sized Carnivora are represented by two premolars, one fragmentary (TNH2-9) and one complete (TNH2-22), but their identification is impossible, even at the genus level. One lower canine could belong to a small-sized felid. A distal part (talonid) of one lower p4 (TNH2-165) is characteristic of Viverridae, possibly Paradoxurus sp.
Large Carnivora are documented by few teeth, among which two canines (TNH2-159 and 182) are fragmentary (Carnivora indet.). One fragmentary m3 and one worn M1 (TNH2-155) are referred to Ursus thibetanus (Fig. 6ai). The M1 size is close to that of Ursus thibetanus kokeni from Yenchingkuo (Middle Pleistocene, China25) and slightly larger than the M1s from Duoi U’Oi (Late Pleistocene, Vietnam139) or Coc Muoi (late Middle Pleistocene, Vietnam28). However, this comparison is based on small data sets (less than three specimens in each site). Although incomplete, two teeth can be assigned to Ailuropoda sp. (TNH2-154 and 152). The assignment of another small fragment to this genus is questionable (TNH2-153).
Ten teeth belong to a cercopithecid (Macaca sp.). Dimensions taken on the most complete teeth (Supplementary Data 2), one p4 (TNH2-167) (Fig. 6af–ag), one M3 (TNH2-162), one M1/M2 (TNH2-205) and one m3 (TNH2-163), fall within ranges of the two middle-sized species M. mulatta and M. nemestrina (Fig. 4 from ref. 149) on M3 and m3; personal data on p4). The well-preserved right p4 (TNH2-167) presents a small anterior basin oriented lingually and a large and rounded posterior basin as in M. nemestrina. Due to the small data set, we cautiously assigned the specimens to Macaca cf. nemestrina. One fragmentary molar also testifies to the presence of an orangutan (Pongo sp.) at the Tam Ngu Hao site.
Eighteen teeth, most worn, belong to a large-sized porcupine (Hystrix sp.) (Supplementary Data 2). Length of two right p4s, two right m1/m2 and four upper molars are on average greater than those of the extant Asian porcupine Hystrix brachyura, and one m1/m2 (TNH2-143) is even larger than those of the other extant species Hystrix indica (Fig. 4 from ref. 150). Overall, dental dimensions fall within the range of Pleistocene Hystrix from several Chinese and Indochinese localities. An assignment to the relatively large-sized species H. kiangsenensis cannot be confirmed.
Comments on associated fauna from Tam Ngu Hao 2 Cave
Despite the poor preservation of recovered specimens, the Tam Ngu Hao 2 cave assemblage is largely similar to those known in southern China and northern Indochina and, to a lesser extent, Java in the Middle Pleistocene25,26,27,151,152. The estimated age range of the fauna (151 +/− 37 kyr) based on the combined US-ESR dating of three teeth fully agrees with the biochronological context given by the faunal assemblage.
Further information on research design is available in the Nature Research Reporting Summary linked to this article.
The mass spectrometry proteomics data generated in this study have been deposited in the in the ProteomeXchange Consortium via the PRIDE partner repository with the dataset identifier PXD018721, including the used proteomic reference database. The hominins teeth and faunal teeth measurements data generated in this study are provided in the Supplementary Data 2 file. The script for Bayesian modelling the Tam Ngu Hao 2 age estimates is provided in Supplementary Fig. 13. TNH2-1 tooth and all the faunal teeth TNH2-2 to TNH2-208 are housed at the National Museum under the responsibility of the Ministry of Information and Culture of Lao PDR. A surface scan of THN2-1 tooth and its EDJ is publicly available in the Human Record archive (https://human-fossil-record.org), register an account and afterwards click the Museum of Lao PDR link on the left hand side of the page). Source data are provided with this paper.
The code used for Bayesian modelling the Tam Ngu Hao 2 age estimates is provided as a Supplementary Fig. 13.
Baab, K. L. In Handbook of Paleoanthropology 2. (eds. Henke, W. & Tattersall, I.) 2189–2219 (Springer, 2015).
Kaifu, Y. et al. Taxonomic affinities and evolutionary history of the Early Pleistocene hominids of Java: dentognathic evidence. Am. J. Phys. Anthropol. 128, 709–726 (2005).
Schwartz, J. H. & Tattersall, I. The Human Fossil Record: Craniodental Morphology of Genus Homo (Africa and Asia), 2. (Wiley-Liss, Inc., 2003).
Athreya, S. & Wu, X. A multivariate assessment of the Dali hominin cranium from China: morphological affinities and implications for Pleistocene evolution in East Asia. Am. J. Phys. Anthropol. 164, 679–701 (2017).
Bae, C. J. The late Middle Pleistocene hominin fossil record of eastern Asia: synthesis and review. Am. J. Phys. Anthropol. 143, 75–93 (2010).
Xing, S. et al. Hominin teeth from the early Late Pleistocene site of Xujiayao, Northern China. Am. J. Phys. Anthropol. 156, 224–240 (2015).
Roksandic, M., Radović, P., Wu, X.-J. & Bae, C. J. Resolving the ‘muddle in the middle’: the case for Homobodoensis sp. nov. Evol. Anthropol. (2021). https://doi.org/10.1002/evan.21929.
Ji, Q., Wu, W., Ji, Y., Li, Q. & Ni, X. Late Middle Pleistocene Harbin cranium represents a new. Homo Species Innov. 2, 100132 (2021).
Li, Z.-Y. et al. Late Pleistocene archaic human crania from Xuchang, China. Science 355, 969–972 (2017).
Wu, X. J. et al. Archaic human remains from Hualongdong, China, and Middle Pleistocene human continuity and variation. Proc. Natl Acad. Sci. U.S.A. 116, 9820–9824 (2019).
Stringer, C. The status of Homo heidelbergensis (Schoetensack 1908). Evol. Anthropol. 21, 101–107 (2012).
Liu, W., Wu, X. J., Xing, S. & Zhang, Y. Y. Human Fossils in China (Science Press, 2014).
Krause, J. et al. The complete mitochondrial DNA genome of an unknown hominin from southern Siberia. Nature 464, 894–897 (2010).
Sawyer, S. et al. Nuclear and mitochondrial DNA sequences from two Denisovan individuals. Proc. Natl Acad. Sci. U.S.A. 112, 15696–15700 (2015).
Chen, F. et al. A late Middle Pleistocene Denisovan mandible from the Tibetan Plateau. Nature 569, 409–412 (2019).
Slon, V. et al. A fourth Denisovan individual. Sci. Adv. 3, e1700186 (2017).
Jacobs, Z. et al. Timing of archaic hominin occupation of Denisova Cave in southern Siberia. Nature 565, 594–599 (2019).
Teixeira, J. C. et al. Widespread Denisovan ancestry in island Southeast Asia but no evidence of substantial super-archaic hominin admixture. Nat. Ecol. Evol. 5, 616–624 (2021).
Larena, M. et al. Philippine Ayta possess the highest level of Denisovan ancestry in the world. Curr. Biol. 31, 4219–4230 (2021).
Demeter, F. et al. Anatomically modern human in Southeast Asia (Laos) by 46 ka. Proc. Natl Acad. Sci. U.S.A. 109, 14375–14380 (2012).
Demeter, F. et al. Early modern humans and morphological variation in Southeast Asia: fossil evidence from Tam Pa Ling, Laos. PLoS One 10, e0121193 (2015).
Shackelford, L. et al. Additional evidence for early modern human morphological diversity in Southeast Asia at Tam Pa Ling, Laos. Quat. Int. 466, 93–106 (2018).
Al Qahtani, S. J. & Liversidge, H. M. The London atlas of human tooth development and eruption. Am. J. Phys. Anthropol. 142, 481–490 (2010).
Bacon, A. M. et al. Late Pleistocene mammalian assemblages of Southeast Asia: new dating, mortality profiles and evolution of the predator-prey relationships in an environmental context. Palaeogeogr. Palaeoclimatol. Palaeoecol. 422, 101–127 (2015).
Colbert, E. H. & Hooijer, D. A. Pleistocene mammals from the limestone fissures of Szechwan, China. Bull. Amer. Mus. Nat. Hist. 102, 1–134 (1953).
Wang, W. et al. Sequence of mammalian fossils, including hominoid teeth, from the Bubing Basin caves, South China. J. Hum. Evol. 52, 370–379 (2007).
Rink, W. J., Wei, W., Bekken, D. & Jones, H. L. Geochronology of Ailuropoda-Stegodon fauna and Gigantopithecus in Guangxi Province, southern China. Quat. Res. 69, 377–387 (2008).
Bacon, A.-M. et al. Nam Lot (MIS 5) and Duoi U’Oi (MIS 4) Southeast Asian sites revisited: Zooarchaeological and isotopic evidence. Palaeogeogr. Palaeoclimatol. Palaeoecol. 512, 132–144 (2018).
Ciochon, R. et al. Dated co-occurrence of Homo erectus and Gigantopithecus from Tham Khuyen Cave, Vietnam. Proc. Natl Acad. Sci. U.S.A 93, 3016–3020 (1996).
Zhang, Y. et al. New 400-320ka Gigantopithecus blacki remains from Hejiang Cave, Chongzuo City, Guangxi, South China. Quat. Int. 342, 35–45 (2014).
Bocherens, H. et al. Flexibility of diet and habitat in Pleistocene South Asian mammals: Implications for the fate of the giant fossil ape Gigantopithecus. Quat. Int. 434A, 148–155 (2017).
Turvey, S. T., Tong, H., Stuart, A. J. & Lister, A. M. Holocene survival of Late Pleistocene megafauna in China: a critical review of the evidence. Quat. Sci. Rev. 76, 156–166 (2013).
Bacon, A. M. et al. A multi-proxy approach to exploring Homo sapiens’ arrival, environments and adaptations in Southeast Asia. Sci. Rep. 11, 1–14 (2021).
Cappellini, E. et al. Early Pleistocene enamel proteome from Dmanisi resolves Stephanorhinus phylogeny. Nature 574, 103–107 (2019).
Welker, F. et al. The dental proteome of Homo antecessor. Nature 580, 235–238 (2020).
Welker, F. et al. Enamel proteome shows that Gigantopithecus was an early diverging pongine. Nature 576, 262–265 (2019).
Bailey, S. E. & Hublin, J.-J. In Anthropological Perspectives on Tooth Morphology (eds. Scott, G. R. & Irish, J. D.) 222–249 (Cambridge University Press, 2013).
Bailey, S. E., Skinner, M. M. & Hublin, J. J. What lies beneath? An evaluation of lower molar trigonid crest patterns based on both dentine and enamel expression. Am. J. Phys. Anthropol. 145, 505–518 (2011).
Skinner, M. M. et al. A dental perspective on the taxonomic affinity of the Balanica mandible (BH-1). J. Hum. Evol. 93, 63–81 (2016).
Olejniczak, A. J. et al. Morphology of the enamel-dentine junction in sections of anthropoid primate maxillary molars. J. Hum. Evol. 53, 292–301 (2007).
Zanolli, C. Molar crown inner structural organization in Javanese Homo erectus. Am. J. Phys. Anthropol. 156, 148–157 (2015).
Zanolli, C. et al. Evidence for increased hominid diversity in the Early to Middle Pleistocene of Indonesia. Nat. Ecol. Evol. 3, 755–764 (2019).
Zanolli, C. et al. The late Early Pleistocene human dental remains from Uadi Aalad and Mulhuli-Amo (Buia), Eritrean Danakil: macromorphology and microstructure. J. Hum. Evol. 74, 96–113 (2014).
Zanolli, C. & Mazurier, A. Endostructural characterization of the H. heidelbergensis dental remains from the early Middle Pleistocene site of Tighenif, Algeria. Comptes Rendus Palevol 12, 293–304 (2013).
Xing, S., Martinón-Torres, M. & Bermúdez De Castro, J. M. The fossil teeth of the Peking Man. Sci. Rep. 8, 2066 (2018).
Xing, S. et al. Hominin teeth from the Middle Pleistocene site of Yiyuan, Eastern China. J. Hum. Evol. 95, 33–54 (2016).
Xing, S. et al. Middle Pleistocene hominin teeth from Longtan Cave, Hexian, China. PLoS One 9, 1–38 (2014).
Pan, L., Dumoncel, J., Mazurier, A. & Zanolli, C. Hominin diversity in East Asia during the Middle Pleistocene: a premolar endostructural perspective. J. Hum. Evol. 148, 102888 (2020).
Morwood, M. J. et al. Further evidence for small-bodied hominins from the Late Pleistocene of Flores, Indonesia. Nature 437, 1012–1017 (2005).
Détroit, F. et al. A new species of Homo from the Late Pleistocene of the Philippines. Nature 568, 181–186 (2019).
Jacobs, G. S. et al. Multiple deeply divergent Denisovan ancestries in Papuans. Cell 177, 1010–1021.e32 (2019).
Slon, V. et al. The genome of the offspring of a Neanderthal mother and a Denisovan father. Nature 561, 113–116 (2018).
Browning, S. R., Browning, B. L., Zhou, Y., Tucci, S. & Akey, J. M. Analysis of human sequence data reveals two pulses of archaic Denisovan admixture. Cell 173, 53–61.e9 (2018).
Gokhman, D. et al. Reconstructing Denisovan anatomy using DNA methylation maps. Cell 179, 180–192.e10 (2019).
Chang, C. H. et al. The first archaic Homo from Taiwan. Nat. Commun. 6, 1–33 (2015).
Wu, X. & Poirier, F. E. Human Evolution in China. A Metric Description of the Fossils and a Review of the Sites. (Oxford University Press, 1995).
Xiao, D. et al. Metric and geometric morphometric analysis of new hominin fossils from Maba (Guangdong, China). J. Hum. Evol. 74, 1–20 (2014).
Rizal, Y. et al. Last appearance of Homo erectus at Ngandong, Java, 117,000–108,000 years ago. Nature 577, 381–385 (2020).
Morley, M. W. et al. Initial micromorphological results from Liang Bua, Flores (Indonesia): Site formation processes and hominin activities at the type locality of Homo floresiensis. J. Archaeol. Sci. 77, 125–142 (2017).
Morley, M. W. et al. Hominin and animal activities in the microstratigraphic record from Denisova Cave (Altai Mountains, Russia). Sci. Rep. 9, 13785 (2019).
Stoops, G. Guidelines for Analysis and Description of Soil and Regolith Thin Sections. (Soil Science Society of America, 2003).
McAdams, C. et al. The Pleistocene geoarchaeology and geochronology of Con Moong Cave, North Vietnam: site formation processes and hominin activity in the humid tropics. Geoarchaeology 35, 72–97 (2019).
Herries, A. I. R. et al. Contemporaneity of Australopithecus, Paranthropus, and early Homo erectus in South Africa. Science 368, eaaw7293 (2020).
Kolobova, K. A. et al. Archaeological evidence for two separate dispersals of Neanderthals into southern Siberia. Proc. Natl Acad. Sci. U.S.A. 117, 2879–2885 (2020).
Aitken, M. J. An Introduction to Optical Dating: The Dating of Quaternary Sediments by the Use of Photon-Stimulated Luminescence (Oxford University Press, 1998).
Hutt, G., Jaek, I. & Tchonka, J. Optical dating: K-feldspars optical response stimulation spectra. Quat. Sci. Rev. 7, 381–385 (1988).
Thomsen, K. J., Murray, A. S., Jain, M. & Botter-Jensen, L. Laboratory fading rates of various luminescence signals from feldspar-rich sediment extracts. Radiat. Meas. 43, 1474–1486 (2008).
Bøtter-Jensen, L. & Mejdahl, V. Assessment of beta dose-rate using a GM multicounter system. Int. J. Radiat. Appl. Instrum. Part 14, 187–191 (1988).
Brennan, B. J. Beta doses to spherical grains. Radiat. Meas. 37, 299–303 (2003).
Wang, W. & Xia, J. The measurement of annual dose from Th series and U series decay chains by thick source alpha counting. Archaeometry1 14, 101–108 (1991).
Guerin, G., Mercier, N. & Adamiec, G. Dose rate conversion factors: update. Anc. TL 29, 5–11 (2011).
Huntley, D. J. & Baril, M. R. The K content of the K-feldspars being measured in optical dating or in thermoluminescence dating. Anc. TL 15, 11–13 (1997).
Huntley, D. J. & Hancock, R. G. V. The Rb contents of the K-feldspars being measured in optical dating. Anc. TL 19, 43–46 (2001).
Prescott, J. R. & Hutton, J. T. Cosmic ray contributions to dose rates for luminescence and ESR dating: Large depths and long-term time variations. Radiat. Meas. 23, 497–500 (1994).
Stokes, S. et al. Alternative chronologies for Late Quaternary (Last Interglacial-Holocene) deep sea sediments via optical dating of silt-sized quartz. Quat. Sci. Rev. 22, 925–941 (2003).
Roberts, H. M. Testing post-IR IRSL protocols for minimising fading in feldspars, using Alaskan loess with independent chronological control. Radiat. Meas. 47, 716–724 (2012).
Rhodes, E. J. Dating sediments using potassium feldspar single-grain IRSL: initial methodological considerations. Quat. Int. 362, 14–22 (2015).
Buylaert, J. P., Murray, A. S., Thomsen, K. J. & Jain, M. Testing the potential of an elevated temperature IRSL signal from K-feldspar. Radiat. Meas. 44, 560–565 (2009).
Murray, A. S., Buylaert, J. P., Thomsen, K. J. & Jain, M. The effect of preheating on the IRSL signal from feldspar. Radiat. Meas. 44, 554–559 (2009).
Thiel, C. et al. Luminescence dating of the Stratzing loess profile (Austria)—testing the potential of an elevated temperature post-IR IRSL protocol. Quat. Int. 234, 23–31 (2011).
Thomsen, K. J., Murray, A. S. & Jain, M. Stability of IRSL signals from sedimentary K-feldspar samples. Geochronometria 38, 1–13 (2011).
Li, B. & Li, S. A reply to comments by Thomsen et al. on ‘Luminescence dating of K-feldspar from sediments: a protocol without anomalous fading correction’. Quat. Geochronol. 8, 49–51 (2012).
Brown, N. D., Rhodes, E. J., Antinao, J. L. & McDonald, E. V. Single-grain post-IR IRSL signals of K-feldspars from alluvial fan deposits in Baja California Sur, Mexico. Quat. Int. 362, 132–138 (2015).
Huntley, D. J. & Lamothe, M. Ubiquity of anomalous fading in K-feldspars and the measurement and correction for it in optical dating. Can. J. Earth Sci. 28, 1093–1106 (2001).
Jacobs, Z., Duller, G. A. T. & Wintle, A. G. Interpretation of single grain De distributions and calculation of De. Radiat. Meas. 41, 264–277 (2006).
Olley, J. M., Murray, A. & Roberts, R. G. The effects of disequilibria in the uranium and thorium decay chains on burial dose rates in fluvial sediments. Quat. Sci. Rev. 15, 751–760 (1996).
Zhou, H., Zhao, J., Qing, W., Feng, Y. & Tang, J. Speleothem-derived Asian summer monsoon variations in Central China. 54-46ka. J. Quat. Sci. 26, 781–790 (2011).
Clark, T. R. et al. Discerning the timing and cause of historical mortality events in modern porites from the Great Barrier Reef. Geochim. Cosmochim. Acta 138, 57–80 (2014).
Ludwig, K. R. User’s Manual for Isoplot 3.75. A Geochronological Toolkit for Microsoft Excel (Berkeley Geochronology Center Special Publication No. 5, 2012).
Cheng, H. et al. The half-lives of uranium-234 and thorium-230. Chem. Geol. 169, 17–33 (2000).
Eggins, S. M. et al. In situ U-series dating by laser-ablation multi-collector ICPMS: new prospects for quaternary geochronology. Quat. Sci. Rev. 24, 2523–2538 (2005).
Joannes-Boyau, R. & Grün, R. Thermal behavior of orientated and non-orientated CO2- radicals in tooth enamel. Radiat. Meas. 44, 505–511 (2009).
Joannes-Boyau, R., Grün, R. & Bodin, T. Decomposition of the laboratory gamma irradiation component of angular ESR spectra of fossil tooth enamel fragments. Appl. Radiat. Isot. 68, 1798–1808 (2010).
Joannes-Boyau, R. Detailed protocol for an accurate non-destructive direct dating of tooth enamel fragment using electron spin resonance. Geochronometria 40, 322–333 (2013).
Grün, R., Athreya, S., Raj, R. & Patnaik, R. ESR response in tooth enamel to high-resolution CT scanning. Archaeol. Anthropol. Sci. 4, 25–28 (2012).
Westaway, K. E. et al. An early modern human presence in Sumatra 73,000-63,000 years ago. Nature 548, 322–325 (2017).
Joannes-Boyau, R., Duval, M. & Bodin, T. McDoseE 2.0 A new Markov Chain Monte Carlo program for ESR dose response curve fitting and dose evaluation. Quat. Geochronol. 44, 13–22 (2018).
Joannes-Boyau, R. & Grün, R. A comprehensive model for CO2- radicals in fossil tooth enamel: Implications for ESR dating. Quat. Geochronol. 6, 82–97 (2011).
Duval, M. & Grün, R. Are published ESR dose assessments on fossil tooth enamel reliable? Quat. Geochronol. 31, 19–27 (2016).
Shao, Q. et al. ESR, U-series and paleomagnetic dating of Gigantopithecus fauna from Chuifeng Cave, Guangxi, southern China. Quat. Res. 82, 270–280 (2014).
Bronk Ramsey, C. Radiocarbon calibration and analysis of stratigraphy: the OxCal program. Radiocarbon 37, 425–430 (1995).
Smith, B. H. Patterns of molar wear in hunter-gatherers and agriculturalists. Am. J. Phys. Anthropol. 63, 39–56 (1984).
Martínez de Pinillos, M. et al. Trigonid crests expression in Atapuerca-Sima de los Huesos lower molars: Internal and external morphological expression and evolutionary inferences. Comptes Rendus Palevol 13, 205–221 (2014).
Turner II, C. G., Nichol, C. R. & Scott, G. R. in Advances in Dental Anthropology (eds. Kelley, M. A. & Larsen, C. S.) 13–31 (Wiley-Liss, Inc., 1991).
Scott, G. R. & Irish, J. D. Human Tooth Crown and Root Morphology. The Arizona State University Dental Anthropology System (Cambridge University Press, 2017).
Spoor, C. F., Zonneveld, F. W. & Macho, G. A. Linear measurements of cortical bone and dental enamel by computed tomography: applications and problems. Am. J. Phys. Anthropol. 91, 469–484 (1993).
Fajardo, R. J., Ryan, T. M. & Kappelman, J. Assessing the accuracy of high-resolution X-ray computed tomography of primate trabecular bone by comparisons with histological sections. Am. J. Phys. Anthropol. 118, 1–10 (2002).
Coleman, M. N. & Colbert, M. W. Technical note: CT thresholding protocols for taking measurements on three-dimensional models. Am. J. Phys. Anthropol. 133, 723–725 (2007).
Maureille, B., Rougier, H., Houët, F. & Vandermeersch, B. Les dents inférieures du néandertalien Regourdou 1 (site de Regourdou, commune de Montignac, Dordogne): analyses métriques et comparatives. Rev. d’archéologie pr.éhistorique 13, 183–200 (2001).
Scolan, H., Santos, F., Tillier, A. M., Maureille, B. & Quintard, A. Des nouveaux vestiges néanderthaliens à Las Pélénos (Monsempron-Libos, Lot-et-Garonne, France). Bull. Mem. Soc. Anthropol. Paris 24, 69–95 (2012).
Olejniczak, A. J. et al. Dental tissue proportions and enamel thickness in Neandertal and modern human molars. J. Hum. Evol. 55, 12–23 (2008).
Olejniczak, A. J. et al. Molar enamel thickness and dentine horn height in Gigantopithecus blacki. Am. J. Phys. Anthropol. 135, 85–91 (2008).
Macchiarelli, R., Bayle, P., Bondioli, L., Mazurier, A. & Zanolli, C. In Anthropological Perspectives on Tooth Morphology: Genetics, Evolution, Variation (eds. Scott, R. G. & Irish, J. D.) 250–277 (Cambridge University Press, 2013).
Durrleman, S. et al. In Medical Image Computing and Computer-Assisted Intervention - MICCAI 2012 (eds. Ayache, N., Delingette, H., Golland, P. & Mori, K.) 223–230 (Springer, 2012).
Durrleman, S., Pennec, X., Trouvé, A., Ayache, N. & Braga, J. Comparison of the endocranial ontogenies between chimpanzees and bonobos via temporal regression and spatiotemporal registration. J. Hum. Evol. 62, 74–88 (2012).
Durrleman, S. et al. Morphometry of anatomical shape complexes with dense deformations and sparse parameters. Neuroimage 101, 35–49 (2014).
Zanolli, C. et al. Inner tooth morphology of Homo erectus from Zhoukoudian. New evidence from an old collection housed at Uppsala University, Sweden. J. Hum. Evol. 116, 1–13 (2018).
Braga, J. et al. Efficacy of diffeomorphic surface matching and 3D geometric morphometrics for taxonomic discrimination of Early Pleistocene hominin mandibular molars. J. Hum. Evol. 130, 21–35 (2019).
Bookstein, F. L. Landmark methods for forms without landmarks: morphometrics of group differences in outline shape. Med. Image Anal. 1, 225–243 (1997).
Gunz, P. & Mitteroecker, P. Semilandmarks: a method for quantifying curves and surfaces. Hystrix 24, 103–109 (2013).
Gunz, P., Mitteroecker, P. & Bookstein, F. L. in Modern Morphometrics in Physical Anthropology (ed. Slice, D.) 73–98 (Kluwer Academic/Plenum Publishers, 2005).
Skinner, M. M., Gunz, P., Wood, B. A. & Hublin, J. J. Enamel-dentine junction (EDJ) morphology distinguishes the lower molars of Australopithecus africanus and Paranthropus robustus. J. Hum. Evol. 55, 979–988 (2008).
Skinner, M. M., Gunz, P., Wood, B. A., Boesch, C. & Hublin, J. J. Discrimination of extant Pan species and subspecies using the enamel-dentine junction morphology of lower molars. Am. J. Phys. Anthropol. 140, 234–243 (2009).
Mitteroecker, P. & Bookstein, F. Linear discrimination, ordination, and the visualization of selection gradients in modern morphometrics. Evol. Biol. 38, 100–114 (2011).
Cardini, A. & Polly, P. D. Cross-validated between Group PCA scatterplots: a solution to spurious group separation? Evol. Biol. 47, 85–95 (2020).
Cardini, A., O’Higgins, P. & Rohlf, F. J. Seeing distinct groups where there are none: spurious patterns from between-group PCA. Evol. Biol. 46, 303–316 (2019).
Dray, S. & Dufour, A. B. The ade4 package: implementing the duality diagram for ecologists. J. Stat. Softw. 22, 1–20 (2007).
Schlager, S. In Statistical Shape and Deformation Analysis (eds. Zheng, G., Li, S. & Szekely, G.) 217–256 (Academic Press, 2017).
Team, R. D. C. R: a language and environment for statistical computing. http://www.r-project.org (2020).
Bookstein, F. L. Morphometric Tools for Landmark Data: Geometry and Biology (Cambridge University Press, 1991).
Rappsilber, J., Ishihama, Y. & Mann, M. Stop And Go extraction tips for matrix-assisted laser desorption/ionization, nanoelectrospray, and LC/MS sample pretreatment in proteomics. Anal. Chem. 75, 663–670 (2003).
Kelstrup, C. D. et al. Performance evaluation of the Q exactive HF-X for shotgun proteomics. J. Proteome Res. 17, 727–738 (2018).
Tyanova, S., Temu, T. & Cox, J. The MaxQuant computational platform for mass spectrometry-based shotgun proteomics. Nat. Protoc. 11, 2301–2319 (2016).
Mackie, M. et al. Palaeoproteomic profiling of conservation layers on a 14th century italian wall painting. Angew. Chem. Int. Ed. 57, 7369–7374 (2018).
Wagih, O. Ggseqlogo: a versatile R package for drawing sequence logos. Bioinformatics 33, 3645–3647 (2017).
Brademan, D. R., Riley, N. M., Kwiecien, N. W. & Coon, J. J. Interactive peptide spectral annotator: a versatile web-based tool for proteomic applications. Mol. Cell. Proteom. 18, S193–S201 (2019).
Vizcaíno, J. A. et al. ProteomeXchange provides globally coordinated proteomics data submission and dissemination. Nat. Biotechnol. 32, 223–226 (2014).
Badoux, D. M. Fossil Mammals from Two Deposits at Punung (Java) (Utrecht University, 1959).
Bacon, A. M. et al. Redécouverte d’une faune pléistocène dans les remplissages karstiques de Tam Hang au Laos: premiers résultats. Comptes Rendus Palevol. 7, 277–288 (2008).
Bacon, A.-M. et al. The Middle Pleistocene mammalian fauna from Tam Hang karstic deposit, northern Laos: new data and evolutionary hypothesis. Quat. Int. 245, 315–332 (2011).
Bourgon, N. et al. Zinc isotopes in Late Pleistocene fossil teeth from a Southeast Asian cave setting preserve paleodietary information. Proc. Natl Acad. Sci. U.S.A. 9, 4675–4681 (2020).
Suraprasit, K. et al. The Middle Pleistocene vertebrate fauna from Khok Sung (Nakhon Ratchasima, Thailand): biochronological and paleobiogeographical implications. Zookeys 613, 1–157 (2016).
Cucchi, T. et al. Taxonomic and phylogenetic signals in bovini cheek teeth: towards new biosystematic markers to explore the history of wild and domestic cattle. J. Archaeol. Sci. 109, 104993 (2019).
Gentry, A., Clutton-Brock, J. & Groves, C. P. The naming of wild animal species and their domestic derivatives. J. Archaeol. Sci. 31, 645–651 (2004).
Wilson, D. L. & Reeder, D. M. Mammal Species of the World, a Taxonomic and Geographic Reference, 3rd edition. (Johns Hopkins University Press, 2005).
Tougard, C. Les faunes de grands mammiferes du Pleistocene Moyen Terminal de Thailande Dans Leur Cadre Pnylogenetique, Paleoecologique et Biochronologique. (Universite de Montpellier, 1998).
Filoux, A., Wattanapituksakul, A., Lespes, C. & Thongcharoenchaikit, C. A Pleistocene mammal assemblage containing Ailuropoda and Pongo from Tham Prakai Phet cave, Chaiyaphum Province, Thailand. Geobios 48, 341–349 (2015).
Hooijer, D. A. Prehistoric and fossil rhinoceroses from the Malay Archipelago and India. Zool. Meded. 26, 1–138 (1946).
Takai, M., Zhang, Y., Kono, R. T. & Jin, C. Changes in the composition of the Pleistocene primate fauna in southern China. Quat. Int. 354, 75–85 (2014).
van Weers, D. J. A taxonomic revision of the Pleistocene Hystrix (Hystricidae, Rodentia) from Eurasia with notes on the evolution of the family. Contrib. Zool. 74, 301–312 (2005).
Norton, C. J., Jin, C., Wang, Y. & Zhang, Y. In Vertebrate Paleobiology and Paleoanthropology (Norton, C. J. & Braun, D. R. eds) 81–100 (Springer, 2011).
Bacon, A. M. et al. A rhinocerotid-dominated megafauna at the MIS6-5 transition: the late Middle Pleistocene Coc Muoi assemblage, Lang Son province, Vietnam. Quat. Sci. Rev. 186, 123–141 (2018).
The team dedicates this work to Mr Thongsa Sayavongkhamdy. We thank the Ministry of Information, Culture and Tourism of Lao PDR for encouraging and supporting our work, marking almost 20 years of collaboration. We thank the authorities of Xon district, Hua Pan Province and the villagers of Long Gua Pa village for their continuous support of our numerous years of fieldwork. We also thank many curators and colleagues who granted access to the comparative fossil and recent hominin specimens for scanning, as well as the online sharing platforms of the Nespos society (http://www.nespos.org) and ESRF Paleontological database (http://paleo.esrf.eu). We acknowledge A. Mazurier and R. Macchiarelli (University of Poitiers), A. Bravin, C. Nemoz and P. Tafforeau (ESRF Synchrotron), P. Bayle and F. Santos (University of Bordeaux), O. Kullmer and F. Schrenk (Senckenberg Museum), F. Bernardini and C. Tuniz (ICTP Trieste), J. Braga and J. Dumoncel (University of Toulouse) for analytical support, microtomographic scanning and sharing of material. We gratefully acknowledge support from the CNRS/IN2P3 Computing Center (Lyon - France) for providing computing and data-processing resources needed for this work. Our thanks also go to Christine Lefèvre, Joséphine Lesur and Aurélie Verguin (Laboratoire Mammifères et Oiseaux, Anatomie comparée, MNHN, Paris) for access to comparative mammalian collections. Warm thanks to Jeremy Kazan (Taxidermie, MNHN, Paris) for having, as usual, wonderfully casted and reproduced the specimen. M.W.M. thanks George Morgan and Mark Keene at Adelaide Petrographics for expertly making the micromorphology thin sections. This research has been funded by the Australian Research Council (ARC) Future Fellowship award (FT180100309) (M.W.M.), the Australian Research Council (ARC) Discovery grant (DP170101597) (K.E.W.), and the Australian Research Council (ARC) LEF Grant (LE200100022) (R.J-B.), the Marie Skłodowska Curie Individual Fellowship (no. 795569) (F.W.). Marie Skłodowska-Curie European Training Network (ETN) TEMPERA, a project funded by the European Union’s Framework Program for Research and Innovation Horizon 2020 (no. 722606) (E.C., J.V.O., P.R.), the European Research Council (ERC) under the European Union’s Horizon 2020 research and innovation programme (no. 948365) (F.W.), the VILLUM FONDEN (no. 17649) (E.C.). European Union’s Framework Program for Research and Innovation Horizon 2020 (no. 819960) (M.M.S.), the Novo Nordisk Foundation (grant number NNF14CC0001) (P.L.R.), the National Geographic Society (NGS-399R-18) (L.S.), the MNHN/Université Paris Diderot/Sorbonne Paris Cité, France (F.D.), the CNRS/Université de Paris, France; Université de Strasbourg, France (A.M.B.). Department of Human Evolution, Max Planck Institute for Evolutionary Anthropology, Leipzig, Germany (A.M.B.) and the Sodipram company (La Compagnie du Lit), France (F.D.).
The authors declare no competing interests.
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Demeter, F., Zanolli, C., Westaway, K.E. et al. A Middle Pleistocene Denisovan molar from the Annamite Chain of northern Laos. Nat Commun 13, 2557 (2022). https://doi.org/10.1038/s41467-022-29923-z