Earliest evidence of human occupations and technological complexity above the 45th North parallel in Western Europe. The site of Lunery-Rosieres la-Terre-des-Sablons (France, 1.1 Ma)

The site of LuneryRosieres la-Terre-des-Sablons (Lunery, Cher, France) comprises early evidence of human occupation in mid-latitudes in Western Europe. It demonstrates hominin presence in the Loire River Basin during the Early Pleistocene at the transition between an interglacial stage and the beginning of the following glacial stage. Three archaeological levels sandwiched and associated with two diamicton levels deposited on the downcutting river floor indicate repeated temporary occupations. Lithic material yields evidence of simple and more complex core technologies on local Jurassic siliceous rocks and Oligocene millstone. Hominins availed of natural stone morphologies to produce flakes with limited preparation. Some cores show centripetal management and a partially prepared striking platform. The mean ESR age of 1175 ka ± 98 ka obtained on fluvial sediments overlying the archaeological levels could correspond to the transition between marine isotopic stages (MIS) 37 and 36, during the normal Cobb Mountain subchron, and in particular at the beginning of MIS 36. The Lunery site shows that hominins were capable of adapting to early glacial environmental conditions and adopting appropriate strategies for settling in mid-latitude zones. These areas cannot be considered as inhospitable at that time as Lunery lies at some distance from the forming ice cap.


ESR dating methodology
For the Lunery deposits, ages were determined using ESR aluminium (Al) centres.Considering the antiquity of the alluvial remnants, titanium (Ti) centres were not used for comparison, as they tend to saturate and underestimate the obtained ages (see details in Despriée et al., 2007Despriée et al., , 2016Despriée et al., , 2017;;Voinchet et al., 2010).
The Al centres of quartz grains are reset by exposure to sunlight during the transport of sediment by rivers (optical bleaching).This bleaching is however always incomplete, even after a long exposure to sunlight, and maximal bleaching occurs after about 6 months exposure (Toyoda et al., 2000).This bleaching empties the Al centres with low activation energy levels (OBAT - Tissoux et al., 2012), but has no impact on those with high activation energy levels (deep centres or DAT).After sediment deposition by the river, the OBAT centres fill up again and can be used for dating the time of deposition.To estimate an age, the portion of the signal of DAT centres must be measured.The ratio between the two types of centres provides information about sediment transport conditions and the relevance of the final results.
The proportion of non-bleachable deep centres was determined by conducting ESR measurements on a bleached aliquot exposed to light from the Dr. Hönle SOL 2 solar simulator.The light intensity received by each aliquot ranged between 3.2 and 3.4x105 Lux, and the samples were illuminated for a duration of 1600 hours.The bleaching rate δbl (%) is then determined by comparison of ESR intensities of the natural and bleached aliquots (δbl= ((Inat-Ibl)/Inat)x100).All the Lunery samples showed bleaching rates of between 41% and 46% (Table S1), which correspond to an average value, commonly observed for sediments transported by the river.
Quartz grains were dated using the standard multiple aliquot additive dose method (MAAD).The 100-200 µm quartz grain size fraction was first extracted from the sediments using the chemical and physical protocol described by Voinchet et al. (2004).The ESR acquisition parameters used were 5 mW microwave power, 1024 points resolution, 20 mT sweep width, 100 kHz modulation frequency, 0.1 mT modulation amplitude, 40 ms conversion time, 20 ms time constant and 1 scan.ESR intensity of the Al signal was measured between the top of the first peak at g=2.018 and the bottom of the 16th peak at g=2.002 of its hyperfine structure (Toyoda and Ikeya,1991;Falguères, et al., 1991 The dose rate was derived from a combination of in situ and laboratory measurements.External alpha and beta contributions were obtained from the radioelement content of each sediment, determined from laboratory high-purity germanium (HPGe) gamma measurements, using the dose-rate conversion factors of Guérin et al. (2011).The k-value of 0.07 ± 0.01 (Bartz et al., 2019), alpha and beta attenuations from Brennan (2003) and Brennan et al. (1991), water attenuation formulae from Grün (1994) were used for age calculation.The gamma dose rate was measured in situ directly at the sampling place using a NaI probe connected to Canberra Inspector-1000 multichannel analyser using the threshold approach (Mercier and Falguères, 2007).The cosmic dose rate was estimated from the equations of Prescott and Hutton (1994), taking into consideration the different phases of alluvial deposition.

Tectonic and climatic conditions of clastic formations in the middle Cher valley during the Pleistocene
Systematic surveys in the middle valley of the Cher, over a length of one hundred kilometres, where it crosses the Berry and Sologne regions, have shown that the preserved so-called fluvial sedimentary formations are stepped from the top to the bottom of the valley slopes.The average ESR ages of these formations confirm that they were successively deposited during different glacial/interglacial cycles during the second half of the Early Pleistocene, then throughout the Middle Pleistocene.This stepping is the consequence of the more or less regular uplift of the Paris Basin in response to the Alpine orogeny.Each incision is ten metres deep, on average, followed by aggradations of around five to six meter The stratigraphy of each of these successive aggradations observed up to the floor incised in the bedrock is constant from bottom to top: -On the floor incised in bedrock, the coarse gravity deposits (diamictons) include pebbles and blocks packed in a gravelly, sandy, sometimes very clayey matrix.The grain size, petrography and weathering of these elements indicate that they come from the alluvium preserved on the interfluves or on the edge of the plateau, as well as from the upper formations of the slope uncovered during previous incisions.The fabrics correspond to deposits by solifluction or gelifluction.The distribution of blocks and pebbles in the volume of the diamictons shows that they were modified by cryoturbation, which also disturbed the bedrock.More than half of the siliceous pebbles show frost cracking affecting the entire mass.
-These diamictons were covered by layers of coarse sand and gravel beds with recognized stratification patterns of fluvial origin: crossed or lenticular bedding, laminations.The sandy layers were then largely eroded, frozen blocks and pebbles highlight the erosion surfaces.New sandy-gravelly fluvial deposits cover them.The top of the fluvial stratigraphy is sealed by new several metre-thick diamictons deposited during the subsequent cycles.

Climatic aggradation of clastic sediments at the site
At the Lunery-Rosière-Usine palaeontological site, the Early Pleistocene alluvial formations deposited on the western slope of the Cher valley have been completely eroded, and alluvia preserved only in a karst well.However, 500m further north, at la Terre-des-Sablons, a quarry work revealed three overlying sandy formations preserved on downthrown blocks of Jurassic limestone (Formations 1, 2, 3 from top to bottom).
Although the top of the block located under formation 3 was lowered by a dozen metres compared to the current topographic surface, it remained horizontal at least over the studied area, and the superposition of alluvia above the limestone bedrock was preserved.The stratigraphic sequence of diamictons / fluvial sands was also observed in formation 3. The base of which includes two diamictons layers deposited on the Oxfordian limestone floor, and uncovered after the end of the incision by Cher River sandy deposits (Unit a).
-Origin of clastic sediments Petrographic determinations indicate that the diamicton materials were reworked from remnants of Neogene alluvia more widely spread on the plateau above the western slope of the valley: same grain size, same petrographic composition, same transport marks.Preserved between the Cher and the Arnon valleys, up to 4 to 5 m thick, these alluvia with fluvial stratifications are made up of coarse sands, gravels and weathered pebbles of quartz, granite, gneiss, and Jurassic silicifications ("chailles"), in a red clayey matrix (Debrand-Passard et al., 1975;Fraisse et al., 1987;Lablanche et al., 1994;Manivit et al., 1994).
In Unit a, the stratigraphic sequences reveal successive erosion-aggradation phases: 1.After incision of the limestone bedrock, the exposed surface was eroded into small basins filled with lenses of coarse fluvial sand loaded with iron pisoliths.2. The limestone floor was then covered by Unit a which is subdivided into three superimposed deposits of coarse elements, from bottom to top; layers 2, 1 and 0. The shape of layer 2 and its preserved terminal lobe suggest a mud flow (Van Vliet-Lanoë, 1995).

-Cryoturbation of Unit a
In layer C2, an area of 20 m 2 served as a test area for a total excavation over its entire thickness in order to observe subsequent disturbances to these deposits and to characterize the taphonomic processes underlying these modifications.Four excavation phases (indexed 1 to 4) were thus recorded between the top of layer 2 and the limestone floor.During each of the four phases, gravel organization was preserved.The exposed surfaces were recorded by zenithal views, in order to obtain a precise image of the frequencies of coarse elements and to position the associated prehistoric objects.A database annexed to the views was created with the coordinates, nature and position (orientation and dip) of each element.
-Phase 1: on the transition surface between the base of layer 1 and the top of layer 2, pebbles longer than 4 cm are generally lying flat; -Phase 2: the stones are still flat, but we note groupings of granules and small stones which form clearly visible ridges.These ridges delimit irregular polygonal surfaces only made up of fine to medium sand, sometimes clayey; -Phases 3 & 4: they correspond to the lower half of layer 2, in which pebbles and blocks are sometimes grouped together on surfaces with an irregular polygonal perimeter; or aligned in a vertical or oblique position at the periphery of the polygons.The spaces between polygons are filled by the same coarse sands and granules forming ridges in d1 (Fig. S1 B). - . Phase 3.These reorganizations into polygons and "nests" of the coarse elements of layer 2, generally bearing frost marks, were observed throughout the thickness of layer 2. This layout may result from cryoturbation phenomena (after Despriée et al., 2017).
Irregularities in the surface of layer C2 were then filled with coarse sands, gravel and iron pisoliths.The absence of fine particles, as well as the illuvial features detected during micromorphological examinations of the sediments, indicate that this surface was leached.This could result from the leaching of the upper surface of layer C2 during thawing, after the exposure of the bases of the largest horizontal stones, limiting the polygonal features observed in phase 1. Above layer C2, the second gravel deposit (layer C 1), 20 to 25 cm thick, contains pebbles and some small cobbles.Fabric measurements seem to indicate deposition by solifluction.At the south-western limit of this deposit, a 40° slope may correspond to the edge of a mud flow (Van Vliet Lanoë, 1995).No specific distribution of pebbles or cobbles was observed in the geometry of this layer 1.However, the large percentage of frost-fractured stones (30 to 50 %) could suggest that layer C1 contained cobbles subject to freeze-thaw action in a previous cold phase, maybe during the aggradation of layer C2.
A limestone debris flow (layer C0), the terminal end of which was also preserved intact, covered the diamicton C1.These debris were observed continuously over a length of more than 10 m, becoming increasingly thicker upstream.The excavation did not reach the end of the deposit.These deposits, known as "limestone stratified screes", were observed on the plateau and on the slope.They are made up of centimetre-sized, angular elements with a flattened triangular section.These cryoclastic deposits are very developed near the site in the Saint-Florent-sur-Cher sector where solifluction phenomena are particularly visible (Lablanche et al., 1984).At Lunery, in the excavation area, the deposits of this layer 0 have retained their original organization and could have been deposited frozen.
-Sandy Unit b Stratigraphic Unit a was covered by fluvial sandy deposits, named Unit b.In this Unit b, the figures of fluvial deposits are very clear.The multiple modes and poor classification of particles correspond to differences in deposition dynamics: low current and settling processes at the base, alternating calm regimes with episodic recovery of competence; finally, successive sequences of coarse or medium sands with beds of gravel indicating a current with variable competence but not capable of moving the coarse elements.Significant modifications were noted in the stratigraphy of this unit b above the karstic features located in the K-L bands.The verticalization of some layers of coarse sand, then their upholding by an unorganized filling seems to indicate a deepening of this well during and after the establishment of the fluvial formation, as was observed in the Somme valley (Antoine et al., 2016;Bahain et al., 2016).This deepening continued, as evidenced by the 50 cm of clay from limestone alteration observed at the bottom of the karst sink-hole.

Palaeoclimatic interpretation
The deposits of Formation 3 of Lunery overlying the Oxfordian limestone bedrock incised by the Cher River during the Early Pleistocene appear to correspond to the superposition of deposits produced after incision during the beginning of the subsequent glacial period (Lefebvre et al.,1994;Antoine, 1994;Bridgland & Allen, 1996;Bridgland 2000).
Hominins were present after the deposition of each coarse diamicton, from which they selected siliceous raw materials.Subsequent cryoturbations reworked the cobbles, then also moved prehistoric artefacts, cores and flakes abandoned on the site.However, these cryoturbations did not completely erase some anthropogenic assemblages of archaeological level 3, containing anvils, hammerstones and flakes.Hominins may have been present during the first aggradation of coarse sediments following the virtual disappearance of plant cover at the beginning of the glacial phase, when the continental ice cap began to develop over northern Europe.At this stage, conditions were not yet very cold to the south, but rainfall was probably abundant.Prehistoric artefacts of archaeological level 2 were, for their part, moved by runoff phenomena.
Similar climatic deposits deposited by gravity and similar cryoturbated features have also been observed in another Early Pleistocene site in the Creuse valley, at Eguzon-Chantôme, Pont-de-Lavaud site (Despriée et al., 2006).On that site, hominins left quartz assemblages on the surface modified by the cold during a glacial stage.The presence of pollen and phytoliths from plants typical of a warm and humid temperate climate indicate that humans arrived during the following interglacial period (Marquer et al., 2011).

Conclusion
In the Centre-Val de Loire region, in the middle valleys of the Creuse, Cher and Loir, coarse solifluction and gelifluction deposits were observed under the bottom of most of the fluvial formations dated to the Early and Middle Pleistocene.Diamictons deposited on the incision floor served as raw material deposits for hominins, who abandoned their artefacts on or around the coarse deposits after use.The stratigraphic position of the prehistoric assemblages indicates that hominins were present during or just after the deposition of diamictons on the incision floor (Lunery), or during the following interglacial (Eguzon-Chantôme, le Pont-de-Lavaud).On these sites, among the most ancient in Europe, evidence of glacial-interglacial cycles already affected the soils, but not very profoundly.Some of the features were fortunately preserved and fossilized by relatively thick fluvial deposits.In all these sites, fluvial sands have been dated by the electron spin resonance method.These sands cover the diamictons and their associated prehistoric industries.Therefore, the age of the periglacial deposits and prehistoric assemblages could be estimated to be older than the sands covering them.

Types and origin of raw materials
The first macroscopic observation of the artefacts unearthed during the archaeological excavation raised several questions about the nature and origin of the siliceous materials used by hominins at Lunery (Table S2): Level Despite the fact that certain scar removal surfaces on cores (33%) and some ventral faces of flakes (20%) are sometimes veiled by iron oxide deposits, two types of siliceous rocks appear to have been chosen: -The first type: about 72 % of the artefacts present cortical surfaces and/or groundmasses containing abundant ooids and bioclasts.Despite extremely varied colours, significant ferruginous permeations and different lateritized aspects (burning aspects), this rock can be compared to chaille-type Jurassic silicifications (= "chailles": Cayeux, 1929;Trauth et al., 1978;Thiry, 1999); -The second type: 28 % of the siliceous artefacts, could not be determined.They contain no ooids or bioclasts, comprise fine or micritic groundmasses, and can be compared to the millstones reported in the local Ludian-Stampian lacustrine limestones, or to Cretaceous flints from the region (Lablanche, 1982;Aubry, 1991;Person et al., 1994).A petrological study was thus required to characterize and locate the geological sources of the materials used.
The petrological study began with sampling 250 cobbles from layers C1 and C2 of the diamicton.The gathered stones presented similar morphologies and alterations to those of the knapped artefacts.Due to the presence of ferruginous argillans on the surfaces, only 210 pieces are sedimentary cobbles, the others are igneous and endogenous rocks.Blocks and cobbles, sometimes with preserved cortical areas, derive from nodules broken as a result of ancient breaks or shocks during transport.Many of them present signs of gelifraction.

Nb % Facies
With Despite the ferruginous deposits regularly covering the surfaces, some stones (42 %) comprised ooids on the preserved cortical areas.In addition, numerous ooids, and /or ossicles are observed on fresh broken surfaces, and also very homogeneous fine or micritic fabrics (Table S3).On the other samples, raw materials show colouring and subsequent transformations, notably burning aspects and ferruginous permeation.These petrographic types require determination by the examination of thin sections.
These observations support the hypothesis that layers C1 and C2 could have served as raw material sources for hominins (Despriée et al., 2017).
. Locally, field surveys failed to find siliceous rocks in the Oxfordian marine limestones exposed on the eroded slopes of the valley and no millstone was found in the lacustrine limestones incised by the Cher.However, blocks and pebbles with the same magmatic, metamorphic and sedimentary petrographic natures and the same alterations were observed in the Pliocene alluvial fans preserved quite far away on the top surface of the limestone plateau and the interfluves.In these remnants, laterization and transport alteration, clearly subsequent to the original diagenesis, were probably acquired during successive tertiary transports and deposits between the original geological site, and the Pleistocene site (Fig. S3).
Regionally, twenty-five kilometres further south, in the Saint-Amand-Montrond cuesta, series of Dogger limestones, crossed upstream by the Cher River, and already reported to contain siliceous nodules, were targeted (Grossouvre, 1885;Lorenz, 1992).One hundred samples of nodules were taken from the marine series of limestones deposited in the Bajocian-Bathonian-Callovian series of

Results for siliceous nodules
Four facies were characterized after the examination of 30 samples of siliceous nodules sampled in the marine Jurassic limestone (Table S4): • Facies 1: Oolitic silicifications.On polished surfaces, numerous well sorted oolites are mixed with some bioclasts.Oolites are floating, or joined, or in well-marked bedding.Their laminae and cores, with diameters between 0.5 and 1 mm are visible.Examination shows diffuse or irregular secondary silicification, cracks filled with silica and spathic breaks.In areas which appear to be resilicified, these oolites are almost no longer visible or not at all, but they are visible on thin sections.
• Facies 2: Entrochal silicifications On polished surfaces; numerous debris of ossicles and some fragments of shells are visible in finegrained silicifications.Ossicles are between 0.5 and 3 mm.Oolites are very rare.On thin sections, oolites are not visible.The silicification of nodules is very regular and no subsequent silica deposits are observed on thin sections.
• Facies 3: Micritic silicifications There are micritic silicifications with no visible texture.The rock can be described as mudstone in which no elements are macroscopically or microscopically visible on polished surfaces.Their appearance is very similar to that of flints.On thin sections, ossicles are always present and oolite core phantoms persist.These micritic rocks are also entrochal and oolitic silicifications contained altered elements masked by recrystallization phases.
• Facies 4: oolitic silicifications with laterization and resilicification In argillite formations, the siliceous nodules are in secondary position, displaced in the upper part of the altered claystones.Nodules are partially lateritized and resilicified.On polished surfaces, remains of original oolitic calcareous cortex are preserved below remnants of a red to black centimetre-thick ferruginous crust.White silica is also visible between the external iron crust and the siliceous nodule.Iron permeance of the periphery of the siliceous rock is visible over 1 to 2 cm.In the fabric, oolites are partially hidden or are no longer visible.On a thin section in the grey to rust coloured silicification, oolites are joined with rare ossicles.The fabric is organized in sequences with large oolites and rare ossicles, and layers of non-joining oolites.Zones with fine contiguous oolites are interspersed in the coarse pasts.The cracks highlighted by the hematite are re-joined.
These microscopic results from nodules sampled in primary geological deposits were compared to the microscopic examination of thin sections carried out on 12 fragments of nodules from layers C1 and C2 and eight thin sections taken from prehistoric cores and flakes.Results are presented in the table below: For samples with no visible elements, analyses by X-ray diffraction (XRD) confirmed that the mineralogical composition of chalcedony cement corresponded to those known for Jurassic silicifications (Trauth et al., 1978).Infrared spectroscopy (FTIR) shows the extent of iron oxide penetration.

Results for lacustrine millstone slabs
After macroscopic and microscopic examination on polished surfaces and thin sections, siliceous millstone was characterized (sites 6 & 7).This lacustrine siliceous diagenetic concentration fossilized the original facies of the different types of limestone deposited in calm and shallow fresh waters.As in the Lunery samples, only homogeneous fine-grained groundmasses were observed, with orange-red coloration, without breccia or vermiculated structures and no cavities (see Despriee et al., 2016Despriee et al., , 2017)).But Characeae oogonia are sometimes observed in micritic fabrics, difficult to distinguish from ooids, but clearly visible on thin sections.

Conclusion
During several phases of the upper Paleogene and Neogene, large wadis with a tropical regime deposited cones of coarse alluviums on the surface of the Berry Champagne plateau dipping southeast/northwest.The fine and coarse alluvium transported from the south towards the north came from the weathered migmatic, metamorphic and volcanic rocks of the northern edge of the Central Massif and the marine sedimentary series of the Triassic and Jurassic of the southern edge of the Paris Basin (map).These fans underwent several phases of transport, laterization, recrystallization, then dismantling (Lablanche et al., 1994).
Since the Lower Pleistocene, after the opening of the Cher tectonic grabens, in response to the recurrence of "glacial-interglacial" cycles, fans covering the plateau were gradually eroded.During the transition phases at the end of the interglacial phase and at the beginning of the glacial phase, solifluction then gelifluction debris flows accumulated coarse deposits at the foot of the slope on the new incision floor.The morphological study of the pebbles contained in these diamictons showed a percentage between 40 and 60 %, depending on the sectors, of frost weathering and frost-fractured cobbles and pebbles.Hominins therefore had to select siliceous materials before knapping.
The rocks chosen by hominins are varied Bajocian-Bathonian siliceous nodules ("chailles"= 80 %), and Ludian-Stampian lacustrine millstone slabs (20 %).Jurassic silicifications contain oolitic, entrochal or micritic groundmasses, sometimes partially or totally lateritized and resilicified.The microfacies of the groundmasses observed on the cores and flakes of the prehistoric assemblages could thus be compared with those of the pebbles accumulated on the site and on the plateau, then with those of the siliceous nodules found in situ in the Oligocene and Dogger geological formations 35 km upstream of the site.
The use of Jurassic nodules is attested in other European Lower Pleistocene sites, such as Barranco Leon and Fuente Nueva 3 (≈1.2 million years old), excavated in the Guadix-Baza basin in Andalusia, Spain.Macroscopic studies of anthropogenic lithic pieces demonstrate the debitage of various "flint" types in colours ranging from grey to beige, water green and orange-green.Micropetrographic analyses attributed these various facies to grainstone and packstone textures at Barranco Leon, and packstone and wackestone at Fuente Nueva 3.All these rocks contain sponge spicules, pedunculate crinoids, fragments of bivalves and some oolites.Chalcedony cement is cryptocrystalline with the presence of iron oxide.The Dogger formations located less than a kilometre from each of the sites are the possible source of various types of knapped small rounded nodules (Toro- Moyano et al., 2010).

Figure S2 .
Distribution by degrees of laterization in the pebble populations of diamicton layers C1 and C2.
their weathered argillites.Twenty samples of millstone slabs were taken from Paleogene lacustrine deposits.

Figure S3 .
Figure S3.Geological location of the cuesta in the Saint-Amand-Montrond area, in southern Berry (rectangle), where siliceous nodules were sampled in seven sites (black stars): 1-5 in Bajocian-Bathonian-Callovian series and 6-7 in Oligocene limestones; Green areas correspond to remnants of Pliocene alluvial fans with igneous, metamorphic and sedimentary rocks (Jurassic and Stampian silicifications)

Figure S4 .
Figure S4.Numbers and percentages of cores and flakes in different types of Jurassic silicifications (Js) and Paleogene millstone (M) characterized in the three archaeological levels at Lunery.

4.
Figure S5.Length/Width and Width/Thickness (mm) of the flakes for the 3 levels

Figure S11 .
Figure S11.Angles (in degree) of the striking platform of centripetal cores (blue) and cores with one striking platform (red) from level 3 The weighted average ESR age obtained for the fluvial sands deposited by the Cher (Formation 3, Unit b) at Terre-des-Sablons is 1,175 ± 98 ka.This age places the deposition of fluvial sediments in the last quarter of the Early Pleistocene.Palaeomagnetism measurements of samples of fluvial sands produced stable and well-defined ChRM directions, with a maximum angular deviation of less than 15°.Only normal polarity directions (looking north and down) were obtained using the thermal or alternating field(Duval et al., 2020).In this terminal part of the Lower Pleistocene, two periods with positive orientation are known: the Cobb Mountain subchron (1,190 ka) and the Jaramillo subchron (1,060 -900 ka).The age of 1,190 ka of the Cobb Mountain subchron, located at the boundary of MIS 36 and 35, is consistent with the median age obtained by ESR.The fluvial sand would have been deposited by the Cher during stage 36 and the occupations would date from the beginning of cold stage MIS 36 after the incision following the MIS 37/36 climate transition.

Table S2 .
Proportions of artefacts with or without ooids, ossicle fragments, shell fragments and undetermined fossils.

Table S3 .
Results of observations after fresh breaks on 42 % of the siliceous sedimentary samples from diamictons C1 and C2, with visible elements.

Table S5 .
Types of butts and flakes in the flaking reduction process.

Table S6 .
Flake-tools and types of blanks for level 3.