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Scientific Reports Volume 11, Article Number: 19665 (2021) Cite this article

South Asia has the youngest Acheulean site in the world, and outdated records are usually limited to sub-humid landscapes. The Thar Desert marks the main adaptive boundary between monsoon Asia in the east and the Sahara-Arabian desert belt in the west, making it a key threshold for studying human ecological adaptation patterns and their influence on behavior, population, and dispersion patterns. Here, we investigated the Paleolithic occupation of the western edge of the South Asian monsoon in Singi Talav, and conducted new timing, sedimentology, and paleoecological studies on the Acheulean and mid-Paleolithic occupied layers. We limit the occupation of the site from 248 to 65,000 years ago. This provides the first direct paleoecological evidence that the landscape occupied by the production population of Acheulean in South Asia is most notably on the main occupation horizon dating back to 177,000 years. Our results illustrate the potential role of the Thar Desert as the ecological and population frontier of the Paleolithic population.

Acheulean technology is characterized by the production of large-scale double-sided tools, especially hand axes and cleavers, which are found in Africa and western Eurasia, and first appeared in about 100 years. It was 1.75 million years ago (ma) in East Africa1 and lasted until about 130,000 years ago (ka)2. During this period, the human population has undergone significant changes, such as geographic expansion 3, 4, 5, population difference 6, and braining 7, 8, 9. By the time the Acheulean technology was finally abandoned, a large amount of population complexity was observed in Eurasian human populations10,11. This includes expanded Homo sapiens 12, 13, 14, Neanderthals 4, 15 in Europe and West/Central Asia, Denisovans 16, 17 in northeastern Asia, and late Homo erectus 18, and in Southeast Asia. Small Flores 19 and Luzon 20 Asians. The problem of paleohuman demography in South Asia has not been well resolved until about the emergence of Homo sapiens in the fossil record. 39-48 ka21, although its geographic location is at the center compared to the range of other recent Eurasian human populations. Only one fossil provides evidence for the early inhabitants of the area-best described as a human population of the Middle Pleistocene, sharing mosaic features with populations in the east and west, which is related to the Asheli technique 22,23. In the absence of fossils, the use of technology from the Asherian era to the mid-Paleolithic era provides important insights into the current debate surrounding the emergence of Homo sapiens in South Asia and its replacement of early human populations.

Archaeological evidence from Attirampakam clearly proves the ancientness of Acheulean settlement in South Asia, which can be traced back to 1.2-1.8 ma24, while Isampur can be traced back to> 1.2 ma25. However, Acheulean's continued existence in late India and its replacement by mid-Paleolithic technology has only recently become a point of contention26. Acheulean technology has been in use until approximately. 212 ka 27,28 peace treaty in East Africa. 190 ka is 29,30 in Arabia, but the youngest Acheulean combination in the world was discovered in Patpara and Bamburi in the Neutron Valley of India, and the age is between 140 and 120 ka2. Between 300 and 200 ka, with the emergence of the Mesolithic and Mid-Paleolitic combination, significant behavioral changes were observed in most parts of Africa and western Eurasia31,32,33. Evidence from a series of locations and regions supports the emergence of South Asian Paleolithic technology quite late, 34, 35, 36, 37, 38 starting from 114 ka, although recent studies from southeastern India are considered to be the earliest global paleolithic Evidence of mid-era technology approx. 385ka39. Therefore, South Asia is a key global region. In this region, there has been a lot of overlap in the use of Asheri and mid-Paleolitic technologies. It is necessary to examine technological innovation models, ecological adaptation, and their relationship with the demographic structure during this time period.

In South Asia, the old Acheulean sites are still scarce, mainly located in the river basins of central and southern India (Figure 1). Among them, the Acheulean sites that are not dated are also abundant40,41. The paleoenvironmental evidence of these locations usually does not exist, but there are a lot of monsoon rains in central and southern India. Although the climate has changed greatly throughout the Pleistocene, it is likely to support a sub-humid environment. Western India marks the boundary of the modern monsoon system. From the Arawali Mountains to the semi-arid to arid regions of the Thar Desert, precipitation has dropped sharply (Figure 1)42. The existence of sand dunes extends far beyond the boundaries of the modern Thar Desert and enters the modern sub-humid zone, which indicates the direct impact of paleoclimatic flux on the area and its potential to destroy human livability in the Paleolithic 43. The occupation of Acheulean, represented by the presence of hand axes and cleavers, and sparsely decorated thin slice tools, was limited to the edge of western India and was mainly related to larger, long-lasting rivers44. At the same time, the mid-Paleolithic occupation was characterized by the use of Levallois technology and modified flakes and dot kits, while seldom used double-sided tools, which are widespread in the region, including the outdated ones that exist in the modern arid core of the Thar Desert Ruins (Figure 1)) 44. Therefore, the transition from Acheulean to the mid-Paleolithic era seems to mark not only a change in stone tool production practices, but also a change in the scope of their deployment environment. Therefore, checking locations on the edges of the monsoon zone is essential to assess the environmental adaptability of the Acheulean population in South Asia.

The map highlights the location of Singi Talav relative to (left) the main South Asian Acheulean station [data: SRTM (NASA)], (upper right corner) and shows its position in the semi-arid landscape on the edge of the monsoon (data: WorldClim.org110) Relative to other Paleolithic sites in the Thar Desert (bottom right), the locations of SGT6 and SGT7 are explained relative to the excavation sites and main landscape features from 1981-85 [Data: ALOS (JAXA)] [Use ArcMap 10.5 (Map made by https://www.esri.com)]. It is worth noting that the Singi Talav Basin and the adjacent Didwana Salt Lake Basin are separated by a linear dune formed in a fault zone of the Balia hills; the excavation of the 16R dune reveals the sedimentary sequence of the dune, indicating that Starting at ~187 ka, a ~18 m dune accumulation occurred here.

Here, we show the results of a new study by Singi Talav (27°23′24.2"N 74°33′10.9"E; Fig. 1) on Paleolithic occupations, which aims to mitigate the direct threat of industrial activity at the site. Lake The Bien site was extensively excavated in the 1980s, and the archaeological combination of the upper 1 m sediments is described as being occupied by the Microlithic (layer 1), mid-Paleolithic (layer 2) and Acheulean (layers 3-5), covering In the deeper lacustrine sediment sequence (layers 6-11) 45, 46, 47, 48 (see SI1). The combinations of layers 3-5 are best described49, although the limited description of the core technology limits the potential to explore the trajectory of change and innovation within these combinations and the overlying mid-Paleolithic (layer 2). Singi Talav's sediment sequence has not been directly dated before, although it is linked to the Amarpura quarry 50,51, where experimental electron spin resonance dating returned a nominal age estimate of 797ka52 from the carbonate-rich sequence ( See SI2). However, considering the experimental issues related to the samples, there was a lack of any demonstrable stratigraphic correlation for about 52 years. The distance between the stations is 2 km53, and the topography between the stations is very different (Figure SI1), and no direct correlation is tenable. We showed the results of Singi Talav's new sedimentology and paleoecological research, and used light-excited luminescence to directly determine the horizon with artifacts. We explored the significance of these results for examining patterns of changes in behavior in South Asia during the Paleolithic period and their relationship to broader trends in Eurasian human demography and paleoecology.

We examined two newly exposed sediment profiles in the Singi Talav area (Figure 2; see "Methods"), revealing common stratigraphic sequences from previous investigations (see SI3). The first location, which we designated as the 0.8 m deep part of SGT6, was immediately adjacent to the previous excavation. Human and non-human activities eroded the edge of the previous excavation. The surface sediments of SGT6 include upper eolian sand containing sparse, soft, small carbonate nodules (1st layer: 0-0.15 m), covering a series of lake sediments. The frequency of carbonate nodules, There are obvious changes in size, induration and bridging, and there are visible changes in the color of the sediment next to it. The second deposit (layer 2: 0.15-0.45 m) is a light gray silty sand matrix that preserves common, small, solid carbonate nodules, and there is a discrete artifact at 0.35 m. It is different from the underlying layer (layer 3: 0.45 – 0.55 m) based on the increase in density, size and compaction of fine carbonate nodules, which also include fresh rock debris artifacts. The fourth layer (0.55-0.75 m) is composed of light gray fine sand to silt sand layer, including denser large carbonate nodules, and sparse artifacts can be seen everywhere, covering the fifth layer (0.75-0.8 m). It is a pink-gray sandy silt rich in powdery calcium, which combines carbonate nodules and rare fine iron nodules to produce a single rock debris.

Singi Talav exposed sediment sequence [SGT6 (top) and SGT7 (bottom)], comprehensive (from left to right) geochronological results, profile photos, sediment log (indicating the location of dating samples), layer identification, Summary statistics of particle size, magnetic susceptibility, loss on ignition results distinguish alternative organic components, total organic matter (TOC) and carbonate, geochemical weathering index (CIA; WIP), stable isotope analysis results of carbonate nodules, and phytolith analysis (Only applicable to SGT7). The 6*, 7*, and 8* layers of SGT7 are roughly equivalent to the previous report, but we use this notation to identify some subtle differences, while all other layers provide a direct match with the previous report. For further descriptions and data sets, please refer to SI3 and SI6.

The gradual changes in the frequency and form of carbonate nodules in the sediment profile are obvious, and roughly consistent with the average increase in the presence of carbonate in the fine sediments, including 9.7% (layer 1) and 24.2% (second layer). Layer), 42.6% (layer 3), 63.3% (layer 4), and 71.5% (layer 5). With the exception of the first layer, the observed total organic content gradually increased, ranging from 1.9% in the second layer to 3.5% in the fifth layer. There is a linear relationship between the magnetic susceptibility results and the combination of organic matter and carbonate in the fine sediments, indicating that the observed changes with depth are related to the size of the mineral composition of the fine-grained sediments, rather than the changes in the source of the sediments . The chemical change index (CIA; average values ​​of 14.66 and 11.6, respectively) and Parker's weathering index (WIP; average values ​​of 17.21 and 13.17) of the first and second layers both showed higher values, and the third layer was sharp Changes (average CIA = 6.61; average WIP = 7.13), the values ​​of the 4th and 5th layers are comparable (the average CIA is 9.57 and 7.49, respectively; the average WIP is 10.62 and 8.1, respectively). The layer 1-5 of SGT6 directly matches the description of the layer 1-5 of the previous research report on the site, including the characteristics of fine sediment grain size and the presence of the ratio of CaCO3, so that there is a strong correlation between these sequences (see SI1 and SI3). ).

SGT7 was located 400 m west of the earlier excavation site, where a deeper sedimentary sequence was revealed, with a maximum depth of 2.35 m, leading to the identification of eight discrete layers. Although the top five layers are more clearly compared with the SGT6 sequence and previous mining, the bottom three layers show different granularity characteristics, which may be caused by different inputs of wind activity. In SGT7, we refer to layers 1-5, which closely match SGT6 and previous excavations, as well as layers 6*, 7*, and 8*, because they recognize that they are roughly equivalent to those excavated before, but there are Some different characteristics. The first layer (0-0.55 m) contains an aeolian fine sand deposit with very rare fine carbonates, and the second layer (0.55-0.65 m) is a reprocessed aeolian sand with more frequent Of carbonate nodules. The change in the size and frequency of carbonate nodules marks the transition to the third layer (0.65-1 m) and the fourth layer (1-1.15 m) and the fifth layer (1.15-1.6 m). At the same time, the powdery calcium The quality lies in the latter. Identified a sharp contact with the 6th* layer (1.6-1.85 m), medium orange-brown silt with dense, firm and large bridging carbonate nodules, covering the 7th* layer (1.85-2.05 m), upward It becomes thicker, with red-brown silt to sand in the middle. The lowest sediment observed (layer 8*: 2.05-2.35 m) is hardened deep red-brown silty sand with hardened carbonate and fine iron nodules. A stepwise increase in the presence of calcium carbonate was observed between the top five layers, followed by the higher but fluctuating levels of the lower layers. For the total organic content, more complex patterns were observed, with distinctly high levels identified in layer 3, while softer peaks appeared in layers 5 and 6*. Except for layer 1, the CIA and WIP values ​​show limited variation throughout the sequence, and at SGT6, the magnetic susceptibility results vary with the mineral composition of the fine-grained sediments, indicating the existence of a single shared sediment source.

Both sites reflect key changes in the sediment sequence previously reported from the site. In particular, the transition from layer 3 to carbonate-rich sediments is very obvious in both locations, which is reflected in the macroscopic presence of carbonates and changes in the composition of fine sediments. The presence of dense powdery calcareous concrete in layer 5 allows close comparison of SGT 6 and 7 and earlier excavations, thus limiting the key archaeological view of the site. Previous excavations have highlighted discrete changes in sedimentation below layer 5, and similar discontinuities were observed below layer 5 of SGT7, despite some divergence from the originally reported sequence, which may represent a roughly similar lateral change in the geomorphic environment . Discrete rather than continuous changes in the sequence may indicate that the sediment deposition at the site is pulsed rather than continuous, and may reflect the intensity of the monsoon. The removal of unconsolidated fine sediments by wind erosion may make the situation worse. complex.

The luminescent samples are taken from the 2nd (0.34 m), 4 (0.57 m) and 5 (0.78 m) layers of SGT6, and the 3 (0.77 m), 5 (1.26 m), 6* (1.63 m), 7* ( 1.91 m) and 8* (2.26 m) in SGT7. The age is calculated based on the potassium feldspar signal, and the range is between 65.14 ± 5.28 ka and 260.21 ± 20.14 ka. The key luminescence dating results are listed in Table 1, and are further detailed in the method and SI.5. The three ages of SGT6 are consistent in stratigraphy, and the measured luminescence signal has characteristics considered suitable for dating, and these characteristics are within the saturation limit of the technology (see SI.5). We set the second layer as 65.14 ± 5.28 ka, the fourth layer as 176.67 ± 16.83 ka, and the fifth layer as 248.14 ± 26.75 ka.

The age of SGT7 varies between 85.27 ± 6.26 ka and 260.21 ± 20.14 ka, and increases with the depth of the sample OSL-ST7-1 to -3. Like SGT6, the signal measured from the SGT7 sample meets the luminescence screening criteria, although some individual signals appear to be saturated (see SI.4). The number of materials that can be used for dating is very limited, and it is impossible to conduct further tests on these samples or use alternative signals for verification (the quartz signal was found to be saturated during the test). Regarding the obvious age inversion at the bottom of the sequence (sample OSL-ST7-5), we believe this is due to the high thorium content measured in this sample (twice the overlying OSL-ST7-3 sample) [Table SI.5]) , May be related to the dense concentration of carbonate nodules in the sediment matrix and the fluctuation of groundwater level. In view of this anomaly, we suggest that OSL-ST7-5 is currently not as reliable as the other luminous ages of the two locations, and note that if the thorium concentration of OSL-ST7-5 matches that of OSL-ST7-3, the resulting age will not be resolved. Age inversion within certainty (see SI.4). We noticed that the ages between the two sites are roughly parallel, with dates appearing in the 2-6 layers* stratigraphic sequence of the two sites, limiting Singi Talav's key archaeological layers and late depositional stages to approximately 65 and at least 260 ka.

We studied the paleoecology of the late Paleolithic and early late Pleistocene sediments in Singi Talav, and used stable isotope analysis of carbonate nodules and phytolith records to clarify the nature of the vegetation at the site and its changing patterns over time ( Figure 2; Method); SI5). Significant comparability can be observed in the stable isotope values ​​between SGT6 and SGT7, both of which exhibit a highly restricted range. The first layer shows the lowest value of δ13C (average SGT6 = 0.3‰; SGT7 = 0.2‰), the second layer (average SGT6 = 1.2‰; SGT7 = 1.8‰) and the third layer (average SGT6 = 1.2‰; SGT7) Step change between = 1.6‰), the fourth layer (average SGT6 = 1.9‰; SGT7 = 2.1‰) and the fifth layer (SGT6 = 2 ‰; average SGT7 = 2.2‰), the highest value appears in the lower of SGT7 Mineral deposit (layer 6 * average value) = 2.5‰; layer 7 * average value = 2.4‰; layer 8 * average value = 2.3‰). These consistently high values ​​indicate the advantages of the C4 plant community. The decrease in δ18O is observed through the SGT6 sequence from layer 1 (average =-4.5‰) to layer 5 (-2.8‰), and from layer 1 (average =-3.4‰) to layer 4 (average = -0.7‰), in SGT7, and in layers 5-8* The average δ18O ranges from -2.1‰ to -2.7‰.

The phytolith combination was only studied from SGT7 (Table SI13), showing good preservation of different diagnostic types, with less enclosed or rusty forms, and poor preservation of Panicoid phytoliths. Limited changes in the D/P index 54 were observed throughout the sequence, except for the obvious peak in the upper sediment of layer 5, indicating an increase in woody vegetation, and the lower level observed is related to the two lowest units. In the C4 grass, the Iph index of 55 indicates that the short type accounts for two-thirds of the 5-8 layer combination, the tall type accounts for 60-75% of the 4-3 layer combination, and the short type accounts for 60% of the second layer combination. And it appears on the first layer in equal proportions. The Ic index of 56 indicates that the grass is dominated by the C4 type in the entire sequence, accounting for 62% to 84% of the grass combination, and is the most common in the 3rd and 4th layers. In contrast, the C3 grass type is the most common in the 5th and 8th layers*.

Therefore, phytolith records can better explain the variability of flower communities than stable carbon isotope records. This may be partly due to the seasonality of warm and dry conditions required for carbonate formation in the monsoon climate to provide a partial, seasonally selective vegetation record, thereby providing a C4 deviation record57. Nonetheless, both agents in both sequences support a clear focus on C4 vegetation, indicating that Paleolithic occupation of the lakeside occurred at the site to survive the dry season and thrive in the warm and humid summer monsoon The grass is dominated.

Only a new collection of stone artifacts was discovered on SGT6 (Figure 3). Weathered artifacts are identified at the contact between the first and second layers, mainly composed of small flakes (n = 12) and broken flakes (n = 7), with a small number of simple cores (n = 5 ), the focus is on thin slices. A discrete artefact layer was found between 0.3 and 0.35 m on the second layer, consisting of larger complete slices (n = 9), larger cores (n = 3), including multi-platform cores, one of which seems It is a weathered and broken centripetal priority Levallois core with sparser flakes (n = 4). A smaller collection of cultural relics was recovered from the thinner sediments of the third layer, including a large multi-platform core (length = 90 cm) and a large simply decorated sheet (length = 68 cm) and four other pieces. The artefact collection on level 4 includes five slices, two broken slices and one complete slice, as well as a disc-shaped nucleus. A complete sheet was recovered from the fifth layer. These findings are consistent with the combination of artifacts recovered from larger and earlier excavations, but the diagnostic technical elements are limited to the second layer of the broken Levallois core, which is 65.14 ± 5.28 ka. The third layer combination is not directly dated on SGT6, but corresponds to the 85.27 ± 6.26 ka age of SGT7. The direct age of the fourth layer combination is 176.67 ± 16.83 ka, and the individual artifacts of the fifth layer can be traced back to 248.14 ± 26.75 ka, which closely matches the corresponding age of SGT7 of 237.44 ± 18.16 ka. The main archaeological sequence of Singi Talav covers the date of the 6th level in SGT7, which is 260.21 ± 20.14 ka.

Artifacts recovered during Singi Talav's new investigation, including (a) multi-platform core (layer 2); (b) double-sided modified sheet (layer 3); (c) discotic nucleus (layer 4) ; (D) Two-sided invasive removal (eroded from the edge of the quarry); (e) finely modified flakes (eroded from the edge of the quarry).

Our research results place Singi Talav's Paleolithic career within a clear timing and ecological framework for the first time. Crucially, our new luminous age directly determines the career dates on site as ~248 ka, ~177 ka, ~85 ka, and ~65 ka. The oldest major occupation identified in Singi Talav (5th floor) is significantly earlier than comparable evidence from other places in the Thar Desert 44 and spans a time frame in which there is no direct dating location in South Asia, but it In Sadab (approximately 290 ka) and Teggihalli (approximately 287 ka) 58, Nevassa (> 350 ka) 59 and Yedurwadi (> 350 ka) 60, as well as the oldest mid-Paleolithic occupation reported by Attirampakam. The larger combination of cuttings from layer 4 proves the denser occupation of Singi Talav, dating back to the early MIS 6 (~ 177 ka). This co-existed with the ancient human activities of 16R Dune 61, and was associated with evidence of Acheulean activities in other places in the Thar Desert (such as Junagadh [Adi Chadi Wao] and Umrethi62; Mahi, Orsang, and Sabarmati Valleys 63, 64, 65) and other places It matches the South Asia at the end of the Pleistocene (for example, Patpara and Bamburi2; Bhimbetka66; Kaldevanhalli-I58), and the presence of mid-Paleolithic technology in Attirampakam39. The 3rd and 2nd floors signify the early occupation of the site by the Late Pleistocene, dating back to ~85 ka and ~65 ka, respectively, which are the same as the nearby 16R dunes (80-40 ka61) and Katoati (96- 45 ka35,67). ), and a series of mid-Paleolithic sites across the Thar Desert and South Asia. Therefore, the dating of Singi Talav's Paleolithic occupations proves the antiquity of West Indian residence and spans a critical time frame for studying the transition from Asheri crossing the subcontinent to the mid-Paleolithic period.

Singi Talav's layers 5-3 are attributed to Acheulean (SI4), which partially reflects the acceptance of early Pleistocene chronology68. The limited available description of the fifth layer combination, its relatively small size, the prevalence of spalling fragments, and the scarcity of large-scale tools cannot directly diagnose the Asheri technology, but given its chronostratigraphic background, this attribution Is consistent. The fourth layer combination contains a high proportion of hand axes (n = 18) and includes meat cleavers (n = 3) and other large cutting tools. Further evidence shows that there is a clear focus on double-sided reduction 49 in the debitage combination. These features are consistent with contemporary The same characteristics of Acheulean come from all over South Asia. The fourth floor of Singi Talav clearly records the late persistence of Acheulean technology in South Asia, which can be traced back to 177 ka, later than the recent Acheulean occupation of Arab 30 and East Africa 27, making it one of the youngest Acheulean sites in the world. The combination is also eye-catching because of the collection of 6 quartz crystals. These quartz crystals were deliberately transported to this location, but there was no clear practical purpose69. Therefore, it is the oldest non-practical item in the South Asian record. The third layer combination includes a small number of hand axes (n = 3), but lacks other clear features that can directly diagnose Acheulean technology (for example, the presence of a cutter), and more attention to core technology. The Acheulean occupation of Singi Talav at 85 ka is consistent with recent models, indicating the late continuity of Acheulean and substantial overlap with the mid-Paleolithic period throughout Asia70. However, the sparse use of double-sided tools and greater attention to different core reduction techniques are now proven to be consistent features of the mid-Paleolithic period in the Thar Desert, such as at 16R Dune 80-40 ka61, the region’s earliest mid-Paleolithic period. Occupation emerged from 114 ka34. Further direct research on this combination is needed to fully resolve whether it exhibits consistent characteristics with other young late Ascheri or old mid-Paleolithic combinations, or whether it exhibits more than the cultural shift currently recorded. Complex feature mosaic. This ambiguity prohibits the designation of the third layer combination as the youngest Acheulean in South Asia or the world.

Our research is the first detailed study of South Asian lake deposits extending to the Middle Pleistocene, including the first comparison of alternative paleo-ecological alternatives to put the Middle Pleistocene archaeological sites in context. The paleoecological evidence of the wet stage in the Thar Desert is mainly limited to the lake records 71,72,73,74,75,76,77 of the Holocene and the end of the Pleistocene. The more extensive paleoenvironmental evidence comes from the Late Pleistocene river sequence 34,63, 78,79 ,80. More limited evidence for the environment in the Middle Pleistocene comes from studies on the activities of Fengcheng 78, 81, 82 and River 83, and this study by Singi Talav goes beyond its chronological order. However, Singi Talav’s MIS 6 occupation coincided with evidence of river activity in the central Thar Desert83. The existence of active lakes and rivers may provide humans with a completely different regional ecological and livable structure, which is in sharp contrast to the constellation of modern beaches and transient or seasonal streams. In the past 187 ± 43 ka, the growth of the upper 18 m of the SW-NE linear dune exposed to 16R Dune 81,84 proved the potential of wind-sand activities to destroy this wet landscape feature during site occupation, and during the Middle Pleistocene, it may be Singi Talav is separated from the larger, adjacent Didwana Lake (Figure 1c). However, phytoliths and stable isotope records indicate that the lacustrine sedimentation stage of Singi Talav supports C4 flower communities that thrive under seasonal hot and humid conditions promoted by the strong summer monsoon regime. More extensive evidence from throughout the Thar Desert supports the Paleolithic occupation pattern, which is associated with comparable flora and is associated with peak monsoon intensity34,85. The accumulation of sediments in the Singi Talav lake and the thriving C4 ecology span the peaks and troughs of monsoon intensity, including incidents of inconsistency between the Arabian Sea and the Bay of Bengal records (Figure 4). This highlights the importance of terrestrial records in addressing the environmental context of human occupations, especially in landscapes characterized by significant changes, such as the monsoon threshold in western India. Our research provides the first direct evidence from South Asia to prove that the Acheulean population directly participates in the landscape at the edge of the monsoon.

High-altitude cave caves (a: Bittoo Cave [India] 110) and ocean core records from the Arabian Sea (b: MD04111; c: Owen Ridge112) and Bay of Bengal (d: Site 758113) and ocean core records illustrate the cross-occupational monsoon change pattern Singi Talav (SGT6: dark green; SGT7: light green) and the main stages of cultural activities in South Asia, including the late Paleolithic (yellow) and the middle Paleolithic (dark blue) 26, Attirampakam the middle Paleolithic (light blue [Note ​​Means that only two combinations exist]) 39 and late Acheulean (red) 2,58,62. Singi Talav’s lacustrine sedimentation stage is related to the prominent peaks and valleys of the monsoon intensity during the glacial period (MIS 8, 6, and 4) that are evident in the Arabian Sea record, highlighting the importance of terrestrial proxy records for understanding broader climate flux patterns. It appears in the landscape of human habitation in the Paleolithic age.

A comparative study of two-sided surfaces at multiple Acheulean sites in South Asia shows that over time, the refinement (defined as the ratio of thickness to width) tends to increase 86. However, the poorly refined double-faced man from Singi Talav's final career in the Middle Pleistocene confuses this pattern. The preferential and invasive spalling of double-sided and double-sided cores, including fragmentary evidence of Levallois technology, was emphasized at the youngest Acheulean site in South Asia86,87. Similar artifacts appear to appear in Singi Talav (Figures 3d, 5), further supporting the recognition of one of the youngest Acheulean groups in the world. This may indicate that the technical practices shared by the late Acheulean population have undergone extensive changes, adapted to the unique ecological challenges at the edge of the Singi Talav monsoon, or both. The occurrence of young Acheulean occupations in western and central India is in sharp contrast with recent reports about the early mid-Paleolithic period in southeastern India, which dates back to approximately 385-172 ka39, indicating approximately overlap. 255,000 years. In Eastern Africa, approximately overlap. Observed between the youngest Acheulean (ca. 212 ka27,28) and the earliest Mesolithic (ca. 300 ka31,88) site in 90,000 years, the fragmentary appearance of Levallois technology in the Acheulean combination appeared in 600 to 500 ka88 ,89 ,90. A comparable ca. An overlap of 60 ka between the youngest Acheulean (ca. 190 ka29,30) and the oldest Middle Paleolithic (ca. 250 ka32) has also been observed in Southwest Asia, where the continuous use of Levallois technology has not been witnessed. sex. East Africa and Southwest Asia provide a fruitful alternative model for the mid-Paleolithic transition from Asheri to South Asia. The former may represent local changes, while the latter is believed to be caused by population turnover. It is worth noting that in both cases, the young Acheulean sites are located in more marginal, semi-arid habitats, which may highlight the ecological structure of Acheulean’s transition to the mid-Paleolithic period. In order to achieve a strong resolution between any alternatives in the South Asian context, it is necessary to further determine the age and excavation of the late Mi Pleistocene sites. This study by Singi Talav also proves the paleoecological background that resolves the major cultural changes in the region Potential importance.

Layer 3 (a) and layer 4 (be) reported from Singi Talav combined layered double-sided core (redrawn from 49).

Acheulean's continued existence in South Asia at the end of the Pleistocene is significant and coincides with major changes in the population and behavior of the entire Eurasian continent. The longevity of the Asherites in South Asia parallels the continued existence of Homo erectus in Southeast Asia, which is usually associated with the initial spread of Asherite technology to Asia40. The genetic record of the Denisovan population also indicates a persistent pattern of population structure, and the genetic infiltration of the discrete Denisovan population in the modern population indicates a different geographic distribution 92,93. Modern South Asians retain important evidence of Denisovan genetic infiltration, contrary to Southwest Asians94, which increases the possibility of Denisovans living in South Asia during the time frame of modern human expansion in Asia. Recent discoveries indicate that the demographic differences of ancient Asian humans in the late mid-Pleistocene have further intensified, and these problems have been further complicated10. Regardless of which ancient human population in Singi Talav produced the Acheulean toolbox at the end of the Middle Pleistocene, they have begun to come into contact with more marginal environments on the western edge of the Asian monsoon and the eastern edge of the Sahara-Arabian desert belt, which is a major biogeography area. The threshold is 95. This ecological resilience is similar to records in Southwest Asia and East Africa. The youngest Acheulean site is located in the arid interior of Arabia or the high altitude area of ​​the Ethiopian Rift Valley. Sometimes found in the mid-Paleolithic/Stone Age sites are less challenging settings , Reflecting the enduring utility of Acheulean toolkits and the adaptability of the human population using them. In Singi Talav, this tenacity led to the late survival of the Acheulean technique, which coincided with the expansion of Homo sapiens to Southwest Asia, immediately before they spread eastward to all of Asia. The biogeographic threshold between the Sahara-Arabian desert belt and the Asian monsoon encountered by the eastward expansion of the population will be further exacerbated by the obvious behavior at the beginning of the Late Pleistocene and the potential demographic boundary, which may carry a series of The interaction between different human groups.

The field survey was conducted in June 2016. The intervention of SGT6 was carried out using hand tools in a 1 × 1 m square to distinguish discrete sediment units, and subdivide the units into 10 cm levels when necessary to ensure any Controlled recovery of artifacts and sieving the sediment excavated through a 5 mm screen. Due to the presence of groundwater, excavation below 0.8 m is prohibited, which is related to the use of old quarries as part of on-site industrial activities. The sediment sequence is sampled at a resolution of 5 cm for various sedimentological and paleoenvironmental studies. An opaque metal tube is knocked into the wall of the section to recover the sample for luminescence dating. After sampling, the intervention is backfilled. In SGT7, mechanical excavators are removing modern silt related to industrial activities and are able to dig out the fresh part of the sediment at the bottom of the modern sump/silt collector. This is to monitor the appearance of archaeological materials, which do not exist. The sediment sequence is sampled at a resolution of 5 cm for various sedimentological and paleoenvironmental studies. The opaque metal tube was knocked into the wall of the section again to recover the sample for luminescence dating.

LPSA: Sieving a single sediment sample (~10 grams) to remove particles larger than 2 mm, and soaking in 1% HCl in a water bath at 90 °C for at least 24 hours to fully release carbonate and break down fines Material. Add pure water to the sample, then centrifuge at 3500 rpm for 13 minutes to decant the excess liquid. Stir the sample on a vortex mixer and use the Malvern Mastersizer 2000 for sub-sampling, choosing from the center of the vortex generated. Use Gradistat96 to generate summary statistics and sediment descriptions.

Weigh a fine sediment sample (~ 10 g; <2 mm) and heat it in a muffle furnace to 105 °C, 400 °C, 480 °C, 550 °C and 950 °C for 6 hours, and let the deposit cool Up to 105 °C for weighing in each interval and calculating the dryness (105 ° C) The material loss ratio and carbonate (950°C) of the sample (97, 98, 99 below). The remaining sample constitutes the total mineral residue, and the total organic carbon includes all materials lost between 105 and 550 °C100.

Use the chclust function of rioja package 101 in R102 to analyze the average value, ranking, skewness and kurtosis of the fine sediment part, and the ratio of organic matter and carbonate part caused by combustion loss (see SI6 for the data), as the analytical model Auxiliary means. Stratum continuity. These results, combined with on-site observations of sediment color, texture and composition (including macroscopic characteristics such as the size and density of carbonate nodules), were used to analyze the stratigraphic profile between sediment units and between SGT6 and SGT7. , And identify the early corresponding layer mining.

The magnetic susceptibility was measured in the laboratory using a Barlington MS3 susceptibility meter and MS3B sensor to analyze a 10 cm3 sample in a plastic tank and weighed on a precision balance to calculate the mass ratio after drying at 105 °C. High (4.6 kHz; HF) and low (0.46 kHz; LF) frequency susceptibility are recorded, so that the percentage of frequency dependent susceptibility (FD%) can be calculated. We determined the linear relationship between the LF magnetic susceptibility value and the proportion of mineral residues in each sample, indicating that the change in the magnetic susceptibility value corresponds to the non-mineral composition of the sediment sample, rather than the change in the source of the sediment.

A sample of 1 cubic centimeter of sediment is completely precipitated in aqua regia in a water bath at 90 °C. Then Perkin-Elmer ICP-OES was used to analyze the sub-samples of the supernatant, and three repeated measurements were taken to generate the average concentration (mg/l) and relative standard deviation (%RSD) in ppm. Parker's aging index (WIP103) is calculated using the molar weight of each element as an oxide, and the formula is as follows: 100 × (2Na2O/0.35 MgO/0.9 2K2O/ 0.25 CaO/0.7). According to the formula: Al2O3/(Al2O3 CaO Na2O K2O) × 100, the chemical change index (CIA104) is calculated using the molar weight of each element as an oxide.

The stable carbon (δ13C) and oxygen (δ18O) isotope values ​​of soil-forming carbonates were analyzed from the entire SGT6 and SGT7 sequences. The rhizomes and nodules selected from the excavated strata are similar to those observed on the beach surface and in the deflated environment of the dune area around Singi Talav, and the formation of powdery or hard calcium observed elsewhere in the landscape sharp contrast. After Blinkhorn and his colleagues34, each level sampled up to 10 individual carbonates where available, and in each case they were combined to form a single sample.

Before pulverizing with an agate pestle and mortar, each soil-forming carbonate sample was rinsed with ethanol to remove any deposits sticking to the nodules. The sample was then dried at 40 °C for 24 hours and then placed in a borosilicate vial. The vial is flushed/filled with helium at a rate of 100 ml/min for 10 minutes. After reacting with 100% phosphoric acid, δ13C and δ18O were measured on the produced gas using the Thermo Gas Bench 2 connected to the Thermo Delta V Advantage mass spectrometer, which is located in the Human History of the Stable Isotope Laboratory of the Archaeological Department of the Max Planck Institute of Science.

Compare the values ​​of δ13C and δ18O with international reference standards (IAEA NBS 18: δ13C -5.014 ± 0.032 ‰, δ18O -23.2 ± 0.1 ‰, IAEA 603: δ13C 2.46 ± 0.018 O, -0.017 ‰, δ13C ± 0.32 ‰) CO8: δ13C -5.764 ± 0.032 ‰, δ18O -22.7 ± 0.2 ‰ and USGS44: δ13C = ~ —42.1 ‰) (each standard n = 3). All standards are registered by the International Atomic Energy Agency and used to calibrate samples using linear regression methods. Repeated analysis of internal MERCK carbonate standards (Merck δ13C -41.3 ± 0.1 ‰, δ18O -13.4 ± 0.0 ‰) shows that the machine measurement error is c. δ13​​C is ±0.1‰, and δ18O is ±0.1‰.

Phytolith analysis was performed by Dr. Sanjay Eksambekar of the Phytolith Research Institute (PRI) in Pune, India. Phytolith extraction is carried out in the laboratory to remove carbonate and nitrate, and then carry out heavy density separation 105. Use the Olympus research microscope to observe and count up to 300 phytoliths, and take micrographs at 45 times magnification, while observing the morphology and preservation. The classification follows Twiss106 and Eksambekar107, and refers to the PRI's extensive South Asian phytolith database.

The samples for luminescence dating were collected by hammering an opaque tube into a clean sediment surface, and opened and prepared in the Oxford luminescence dating laboratory under soft orange light conditions. Laboratory processing follows standard procedures (for example, 34) to separate potassium-rich feldspar particles for measurement. The infrared signal after the elevated temperature measured from a very small aliquot of sand grain size (1 mm in diameter) is used for equivalent dose measurement, the dose rate is derived from the radionuclide concentration determined by inductively coupled plasma mass spectrometry . Use DRAC108 for final age calculation. Luminous dating is discussed in more detail in the supplementary information.

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We thank Anna University Chennai for providing logistical support and arranging all necessary permits to carry out this work. The field survey and analysis costs were partly supported by research grants provided to JB by the DM McDonald Trust (Macdonald Institute of Archaeology, University of Cambridge) and the Leakey Foundation. JB thanks Chris Rolfe, Laura Healy, Steve Boreham, and the Geography Science Laboratory of the University of Cambridge’s Department of Geography for their support and use of the geoarchaeological research facility. PR and JI thank the Max Planck Society for funding.

Open access funding enabled and organized by Projekt DEAL.

Pan-African Evolution Research Group, Max Planck Institute for Human History Sciences, Jena, Germany

Department of Geography, Centre for Quaternary Studies, Royal Holloway, University of London, UK

Institute of Marine Management, Anna University, Chennai, India

Oxford University School of Geography and Environment, Oxford, UK

Department of Archaeology, Max Planck Institute for Human History Sciences, Jena, Germany

Patrick Roberts and Jana Ignat

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JB and HA conducted field investigations, laboratory analysis was conducted by JB, JD, PR, JI, and all authors wrote and reviewed the manuscript.

The author declares no competing interests.

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Blinkhorn, J., Achyuthan, H., Durcan, J. etc. Chronology and ecology of late Acheulean and mid-Paleolithic occupations that bound the margins of the monsoon. Scientific Representative 11, 19665 (2021). https://doi.org/10.1038/s41598-021-98897-7

DOI: https://doi.org/10.1038/s41598-021-98897-7

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