The Kenya Rift is regarded as one of the most important regions for the study of Pleistocene mammals in Africa and the evolution of early hominins, with a notable concentration of fossil and archaeological sites (Figure 1). This apparent association between Rift environments and finds of early hominins has given rise to the notion that there may be a causal relationship between the two phenomena, with the distinctive dynamics of rifting acting as a key agent in evolutionary change through one of three possible processes: (1) directly at a macro-geographical and temporal scale through the introduction of major barriers that have served to isolate populations along divergent evolutionary pathways (vicariance hypotheses, Coppens, 1994; Lewin & Foley, 2004); (2) indirectly by amplifying spatial and temporal variability in climate and vegetation (hypotheses of mosaic environments and variability selection, Potts, 1996, 1998; Kingston, 2007; Maslin et al., 2014; Trauth & Maslin, 2009); or (3) directly but at a more localised spatio-temporal scale by the creation of a complex and dynamic regional topography that afforded opportunities for the evolution of the distinctive human niche with its emphasis on meat-eating, bipedalism and an extended period of juvenile dependency (the complex topography hypothesis or tectonic landscape model, King & Bailey, 2006; Reynolds, Bailey & King, 2011; Winder et al., 2013). However, establishing robust correlations between environmental variables, especially features of the physical landscape, and distributions of fossil or archaeological sites has well-known difficulties: of accurately reconstructing ancient landscape features in regions subject to ongoing geological change; of biases introduced by differential deposition, preservation, exposure and discovery of bones and stones; of chronological correlation between disparate and stratigraphically unrelated features; and of integrating processes that operate over widely divergent spatio-temporal scales. Faced with difficulties that can seem insuperable, one can either admit defeat, or seek to untangle some of the confounding variables by more detailed investigations of specific regions on a case-by-case basis, aided by known sites of fossil and archaeological remains where available.
In this paper we examine the Central Kenya Rift, in particular the Nakuru-Elmenteita-Naivasha region and its adjacent flanks (Figures 2 and 3). We choose this region because it is relatively compact, it is easily accessible for ground-based survey work, it benefits from a number of detailed and already published studies of the geology, tectonics and climate, and it has some record of Lower Pleistocene archaeology, which though not as abundant or detailed as for other regions of the Rift, comprising mainly the site of Kariandusi, provides a point of departure for examining archaeological material in its wider regional context. We take the complex topography hypothesis as a starting point and present this study as part of an ongoing programme of mapping and research that is intended to extend ultimately to other comparable regions in the Kenyan and Tanzanian Rifts and elsewhere.
We describe our approach as landscape research, but emphasise that it differs in significant ways from the well-established tradition of landscape analysis commonly applied in the study of Plio-Pleistocene deposits in the African Rift (e.g., Isaac, 1977; Isaac & Harris, 1978; Bunn et al., 1980; Kroll, 1994; Stern, 1994; Blumenschine & Peters, 1998; Potts, Behrensmeyer & Ditchfield, 1999; Kingston, 2007; Blumenschine et al., 2012). For the most part, these studies have focused on stone artefacts and faunal materials in relation to their immediately surrounding sediments and surfaces at a spatial scale of hundreds of metres to kilometres, with the emphasis on localised distortions of the record by sediment accumulation and erosion, and on reconstruction of environmental features such as vegetational and palaeoclimatic indicators. Widening the geographical scale of such an approach has necessarily been hampered by problems of time-averaging, stratigraphic discontinuities between different locations, and the difficulties of extrapolating proxy environmental variables over larger areas. Here, we offer an alternative, and to a large extent a complementary approach that addresses the problems of landscape reconstruction at a larger geographical scale, taking account of geological changes in landforms, but one which is also sensitive to regional and local variability. In this way, we aim to create a different type of framework within which to interpret the distribution of fossil and archaeological remains, and add value to results derived from well-established techniques of lithic, faunal, palaeoclimatic and palaeovegetational analysis.
The aims of this paper, then, are to:
We first provide a general introduction to the geological and tectonic history of the region and its principal environmental and archaeological features. We then describe the methods we use to create maps, with particular emphasis on edaphic analysis, and present an analysis of the key topographic and edaphic features that are relevant to routes of movement and access for large mammals, with particular attention to the impact of fault scarps and the history of changes in lake level. Finally, we discuss the Kariandusi archaeological site within this regional framework, show how its attractions as a locus of repeated hominin activity have varied with changes in topography, especially in relation to changes in lake level, and consider the wider implications of these results.
The region has typical features of an asymmetric rift with progressively uplifted flanks reaching heights of ~4000m asl in the Aberdare Range to the east, and ~3000m asl in the Mau escarpment to the west, and down dropping of the central basin, with its floor at about 1800m asl, accompanied by faulting and volcanic activity. Rifting is aligned on a NNW–SSE axis and was active in the late Miocene, between 12 and 6 Ma BP, with further spells of activity between 5.5 and 3.7 Ma, and again at about 2.6 Ma, when the 30-km-wide Kinangop Plateau and the 40-km-wide inner rift depression were formed (Baker, Mitchell & Williams, 1988; Baker et al., 1971; Baker & Wohlenberg, 1971; Clarke et al., 1990; Roessner & Strecker, 1997; Strecker, Blisniuk & Eisbacher, 1990). The Aberdare Range is separated from the inner rift by the Sattima fault, and the Kinangop plateau is a major relay ramp bounded by the Sattima fault to the east and the Kijabe fault and multiple faulting to the south-west (Figures 2 and 3).
The inner rift was subsequently covered by trachytic, basaltic and rhyolitic lavas and tuffs and continues to be cut by normal faulting around a central axis (McCall, 1967; Clarke et al., 1990; Strecker, Blisniuk & Eisbacher, 1990). A change in the direction of extension in the middle Pleistocene has been proposed, with the development of NNE striking normal faults linked by complex transfer zones, and reactivation of some older faults on the new alignment (Bosworth & Strecker, 1997; Strecker, Blisniuk & Eisbacher, 1990; Zielke & Strecker, 2009). The young structures of the inner rift are accompanied by late-Pleistocene to Holocene volcanoes, such as Menengai, Eburru, and Longonot, and some smaller rhyolitic domes and basaltic lava flows. As a consequence, the present-day inner rift has become compartmentalized into smaller lake basins, principally the Nakuru-Elmenteita and Naivasha basins, separated by normal faults and intervening volcanic structures.
The region is dominated by volcanic rocks, and volcaniclastic and lacustrine sediments (Figure 4). The volcanic rocks are predominately lavas and pyroclastic deposits from the Late Miocene to the present (McCall, 1967; Baker et al., 1971; Baker, Mitchell & Williams, 1988). The oldest volcanic units are Late Miocene plagioclase-rich basalts of the Aberdares and Mount Kipipiri. Early Pliocene basalts and phonolites outcrop along the Sattima fault escarpment and the northern part of the Aberdare range. The Kinangop plateau is mostly Pliocene and Pleistocene tuffs and ignimbrites with trachytes to the south and north. The Mau escarpment to the west mainly comprises welded and non-welded ignimbrites of the upper and lower Mau sequences, the source of which is probably in the inner rift, buried by younger deposits (McCall, 1967; Leat, 1991). Basalts dominate the Sattima fault, Mount Kipipiri, and the Aberdare range. South of Lake Elmenteita small rhyolitic to basaltic volcanic cones and Late Holocene basalt flows form the most recent volcanic complex of the area.
The present-day topography is dominated by the tectonic history of the region. Principal pathways of movement mainly run parallel to these major faults, around and across the rift floor and on the Kinangop plateau, with major barriers to east–west movement in most places. The Kenya-Uganda railway although now of little importance, had a vital role in developing the present-day economy of the region and the growth of the towns of Nakuru, Gilgil and Naivasha, and its route across the edge of the rift flanks and the inner rift indicates some of the easiest pathways of movement on the eastern side of the basin. Also, an eastern branch line of the railway used to extend eastwards up onto the flank to near Lake Ol Bolosat giving access to the Kinangop plateau.
The region hosts many small lakes ranging from fresh water to highly alkaline, a variability determined by catchment size (Figure 2b). The fresh water lakes of Baringo and Naivasha have large catchment areas, while those of alkaline Bogoria and Elmenteita are very small. At present the lakes have no outlets and are sensitive to even small changes of climate, exposing towns like Naivasha and Nakuru to risk of flooding. Nowhere within the rift receives water from outside, with rivers flowing away to the east or west down the outer rift-shoulders of the Aberdare and Mau escarpments respectively.
The lakes have a complex history of variations in size, lake level and water composition, determined in part by climate change and partly by tectonic movements (Bergner et al., 2009). Over the past 1 million years, there have been periods when lake levels were substantially higher than present, with important implications for the interpretation of animal movements, considered in more detail below.
Lacustrine sediments occur predominantly in the Nakuru-Elmenteita, the Naivasha and the Baringo basins, and to a smaller extent around Lake Ol Bolosat in the NE part of the Kinangop plateau. The basin fill usually consists of Mid-Pleistocene to Holocene lake sediments interbedded with volcanic ash and pyroclastic deposits (McCall, 1967; Bergner et al., 2009).
Because of the sharp variations in altitude and geology, the Rift exhibits marked variations in climate, vegetation, and land use (Bergner et al., 2009; Hesslerová & Pokorný, 2010; Were, Dick & Singh, 2013). Land at high altitude on the rift flanks is characterized by a perennially cool and humid climate with annual rainfall of up to 3000 mm per year. This climate supports forest cover and the development of thick soils, but much of the forest has been cleared for agriculture and settlement (Hesslerová & Pokorný, 2010), and a major part of Kenya’s agricultural output occurs in these regions, particularly tea and coffee. Conversely, the rift floor is characterized by an arid climate with a short rainy season, poor soil development and an annual rainfall of about 500 mm, particularly in the southern part of the inner rift. Other cash crops include, fruit, vegetables, cotton and flowers, including a concentration of intensive production in the Naivasha basin with huge poly-tunnels and artificial irrigation. Maize and beans are grown for local consumption, and the principal livestock are cattle, sheep and goats.
There are almost no Plio-Pleistocene fossil remains from the immediate region, and details about large-mammal populations before the agricultural era can be inferred only approximately by analogy from adjacent regions of the Kenya Rift (Maglio & Cooke, 1978; Potts, 1994; Turner & Antón, 2004; Bobe, Alemseged & Behrensmeyer, 2007; Bobe & Leakey, 2009), from Late Pleistocene and Holocene rockshelter-deposits on the Mau escarpment (Marean, 1992), and from historical and present-day observations. Hippo still live in the basin today and elephants were present within living memory, while the occurrence of buffalo, zebra, eland, hartebeest, gazelle, klipspringer, antelope and reedbuck in the Hell’s Gate National Park gives some indication of what was once more widely available (Kenya Wildlife Service, 2015). We infer that a full suite of African large mammals would have been available as prey for hominin exploitation, subject to variations in topography, climate and forest cover, but do not attempt a more detailed analysis, since our aim here is to identify general topographic and edaphic constraints on large mammal movements rather than to attempt detailed habitat reconstructions and biogeographic distributions for specific taxa that cannot be corroborated by any currently available evidence.
Only one archaeological site from the Lower-Middle Pleistocene is known in the region we are considering, and that is the Acheulean biface site of Kariandusi with an age bracketed between 0.73 and 0.98 Ma (Gowlett & Crompton, 1994; Leakey, 1931a; Shipton, 2011). The nearest comparable Acheulean site is Kilombe, but that lies further north, where much of the surrounding terrain is blanketed by volcanic material that post-dates the occupation of the site (Figure 4), limiting what can be said about its original landscape setting (Bishop, 1978). Other material of significance but of very much later date is a series of MSA sites and LSA rockshelters on the Kinangop Plateau, full details of which remain unpublished (Lahr, 2015; Waweru, 2002), and the rockshelter of Ekapune Ya Muto above the Mau escarpment, with a long stratified sequence extending from MSA through LSA, including some of the earliest dates, estimated at ~ 50,000, for the LSA in Africa, and later deposits of Neolithic and Iron Age date (Ambrose, 1998). Another group of sites on or close to the rift floor includes Gamble’s Cave and Hyrax Hill, where the cultural material is mainly post-Pleistocene in age, belonging variously to the Later Stone Age (LSA), Neolithic or Iron Age.
The mapping of roughness provides a method to identify and map barriers of greater or lesser extent such as fault scarps and cliffs that would have constrained patterns of movement and access for large mammals. For this region, we derive roughness from DEMs making use of SRTM30 data and ASTER GDEM (a product of METI and NASA) (Bailey, Reynolds & King, 2011), figure 19). This is supplemented by field observations. For the mapping of lake palaoeshorelines, we draw on the published literature on changes of lake level (Trauth et al., 2005; Bergner et al., 2009), supplemented by our own field observations
For the edaphic analysis, we have selected soil and vegetation samples from a representative selection of different lithological and sedimentary units, basing our selection on field observation and geological maps. We excluded regions with an agricultural overprint and severe recent deforestation such as the southern Mau escarpment and Eburru forest to avoid disturbance from agricultural fertilizers and other anthropogenic modifications to the soil composition. We took soil samples using standard protocols provided by KALRO (Kenya Agricultural and Livestock Research Organisation). For thin soils, we generally sampled the uppermost horizon (<25cm). Soil and plant tissue analysis was carried out at the KALRO laboratories (Kübler et al., 2015).
During two field seasons in 2013 and 2014, we collected a total of 163 soil samples and 160 plant tissue samples (Figure S1) in the Kenya Rift from Lake Magadi in the south to Lake Baringo in the north. In this paper, we show results for 75 soil samples and 75 plant tissue samples for the the Nakuru-Elmenteita-Naivasha basin and the Kinangop plateau (Figures 2 & 3, Appendix Figure S1). All samples were tested for concentration of the following trace elements and nutrients: calcium (Ca), copper (Cu), iron (Fe), manganese (Mn), magnesium (Mg), nitrogen (N), potassium (K), sodium (Na), phosphorus (P), and zinc (Zn). Further, soil samples were tested for pH-value, electrical conductivity, and total organic carbon (Table S1. Sample locations and coordinates are shown in Figure S1 and Table S2, respectively). We additionally took water samples from springs and boreholes around Lake Elmenteita to test for fluoride (Table S3) since excess fluoride can be a major problem, resulting in widespread tooth fluorosis (Moturi, Tole and Davies 2005) and bone deformation (rickets) in humans and cattle (Thacher et al., 2006).
A map of roughness, with slopes greater than 15° indicated by dark shading (Figure 3), highlights the constraints on access, whether for large animals or modern motor vehicles. The multiple faulting, especially on the Kijabe and Sattima fault escarpments, presents major barriers to such movements. The Kinangop Plateau is an extensive area of smoother terrain confined to east and west by these fault scarps; its north-western border is also dissected by deeply incised rivers, and its south-eastern border comprises complex faulting and rough topography, making the plateau an enclosed area with very limited points of easy access, the easiest route to and from the rift floor being via the Kariandusi River (Figure 5). According to information from the heads of pastoral families in the area, female hippo are reported to migrate today along this route between Lake Elmenteita and Lake Ol Bolosat to protect their young from aggressive males. In the past, elephants are also reported to have found a route to reach Kinangop. On the western side of the rift the Elgeyo-Mau escarpment represents a barrier to movement as do north–south incised valleys further west on the flank. Apart from these obstacles, movement within the lake basins is largely unrestricted.
There is abundant evidence for higher lake levels. Lake beds can be readily identified on satellite images (e.g. Figure 2b) or Google Earth, and have been extensively studied by Trauth et al. (2005) and Bergner et al. (2009). These authors are mainly interested in climate change rather than palaeotopographic reconstruction and therefore pay most attention to identifying high lake stands. However, they suggest that semi-quantitative information about intermediate levels can be determined from sediment cores. Interpretation of these is complicated by tectonic controls as well as climatic ones, but they indicate at least three episodes of highest lake levels associated with wetter climate over the past one million years: at ~1 ma, 150–60 ka, and 15–4ka. It is possible that Lake Nakuru, Elmenteita and Naivasha formed one lake during times of high lake level but volcanic topography separates them today and conceals any clear evidence that they were once joined (Figure 4).
High lake levels greatly reduce the area of easily accessible grazing or browsing land but do not block movement along lake edges. A major exception is near to the Kariandusi River when the lake reaches a level of 1880m or higher. The steep slopes and cliffs north of the Kariandusi River make any movement along the shoreline impossible (Figure 5). Movement remains difficult until the level has dropped to 1860m and below, when full access is restored. Any movement to and from the north during high lake levels would have to use an inland route as indicated in the Figure. Only one route is possible and is today followed by the railway line and crosses the Kariandusi River close to the Kariandusi archaeological site.
Soils in the study area form on volcanic bedrock (basalt, phonolite, trachyte), volcanic ash and pyroclastic deposits (trachytic, pantelleritic, rhyolitic) and on fluvial and lacustrine sediments. Soil mapping and sampling revealed that on lake beds and trachytic tuffs of the Kinangop plateau, soils are mainly thin (thicknesses above regolith < 50cm). Deep red soils occur on the basalts of Mount Kipipiri, and in the foothills of the Aberdare Range, along the Sattima escarpment, as well as on volcanic ash and pyroclastics of the Mau escarpment and the Eburru forest. Most of the places with deep soils were previously forested but are now associated with intensive agriculture (Hesslerová & Pokorný, 2010; Were, Dick & Singh, 2013). Deep red but strongly weathered and acidified soils dominate the normal faulting complex north and northeast of Kariandusi as well as the edges of the Sattima fault and Mount Kipipiri (Mireri, 2005; Muchena & Gachene, 1988).
The results show that the nutrient distribution in soils of the study region is very heterogeneous. Whereas levels for Fe, Mn, and K are moderate to high in almost all soil and vegetation samples (Figures S2a, S2b, Table S3), other nutrient levels show strong variations throughout the study area. Calcium levels in all soil samples are moderate to high. In vegetation samples, however, Ca is mainly deficient except in samples from basaltic soils south of Mount Kipipiri, river sediments downstream of Mount Kipipiri and on some tuff soils of the Kinangop plateau and the Rongai region (Figure 6a, Table S3). Magnesium levels are moderate to high in all soil samples. Vegetation samples, however, reveal mainly low Mg levels, with the exception of some samples taken from Mount Kipipiri and Sattima basalts, and Kinangop tuffs (Figure 6a). Copper levels are low in a large number of soil samples from lake beds around Elmenteita, and tuffs from Eburru and south of Rongai. In vegetation samples, Cu levels are high in all samples (Figure 6b). Soluble phosphate levels are low in almost all soil samples and moderate in most vegetation samples (Figure 6b). Exceptions are high phosphate levels in soil samples from the Sattima escarpment on basaltic soils and on the foothills of Mount Kipipiri on soils that consist of a mixture of basaltic rocks and ignimbrites. Nitrogen (N) levels are moderate in most soils, except in some soils around Elmenteita and Naivasha with low N levels. In almost all vegetation samples N occurs in moderate levels (Figure S2b). Sodium (Na) is low in most vegetation samples and moderate only in some samples from the Kinangop and Rongai tuffs. High Na levels in vegetation occur in lake beds north of Lake Elmenteita, on Mount Kipipiri basalts and on Mau tuffs. In soil samples Na levels are mainly moderate (Figure S2c). Zinc (Zn) occurs in moderate to high levels in all plant samples. Some soils from the Kinangop tuffs are deficient in Zn (Figure S2c). Fluoride levels were very high in all samples (Figure S3) and for Lake Elmenteita 26.44mg/l, exceeding the recommended upper limit of 1.5mg/l by more than 17 times (WHO, 2004, Table S3).
It is noteworthy that, for both Ca and Mg, levels are moderate to high throughout but almost all samples of vegetation lack both nutrients in many places. A reason for this may be that successful uptake of these nutrients is only possible if they are present in the soil in the right ratio (Schulte & Kelling, 1985).
The results of the edaphic analysis are combined with topographic information to highlight in a more detailed way those areas that can be exploited by large animals, particularly those moving in large groups or herds (Figure 7).
The most striking feature is the patchy distribution of the most favourable categories, with areas characterized by rough topography and poor edaphics dominating the region. These areas would not necessarily have been devoid of animals but are likely, at best, to have been used intermittently, by smaller numbers of animals, or in transit between edaphically and topographically more attractive areas. The best edaphics are confined to the upper rift flanks of the Kinangop Plateau and the Mau escarpment, with smaller patches on the rift floor near Lake Baringo and Lake Elmenteita. The latter is the result of recent (mostly Holocene) volcanic activity and cannot be extrapolated to earlier periods. Areas of moderately good, but variable, edaphics are on the rift floor and on the Kinangop Plateau.
Today, the lake shores provide the most topographically accessible grazing over wide areas. Soils are potentially attractive for animals, with high Ca, Mg, Ca and K contents, but these advantages are offset by other factors. The vegetation growing on these soils often has low Ca and Mg levels, as noted earlier, and geophagia (the practice of eating soil-like substrates) is common today in this part of the Kenya Rift for both humans and animals (Davies, 2008). ‘Salt licks’ at places where lake beds are exposed are an important alternative source of nutrients, and sacks of mineral salt are extracted from these lake-bed outcrops, notably in the quarry below the Kariandusi site, and distributed to farmers more widely in the region to supplement cattle feed. Soils formed on the lake sediments are also usually shallow and sensitive to erosion and have reported low copper and cobalt content (Maskall & Thornton, 1996). This is a particular problem for ruminants as the bacteria exploited by their digestive systems depend on these minerals. Without them, the animals cannot process food and starve. Such cases are reported repeatedly by cattle farmers of the Nakuru region where the disease is known as Nakuruitis.
Lakes Nakuru and Elmenteita are now highly saline and are not a suitable freshwater source for animals. Some drinkable water comes from hot springs in the multi-faulted region to the east of the basin (Figure 3). However, our measurements show very high fluoride levels around Lake Elmenteita (Figure S3).
In summary, the areas around the lake basins of the inner rift provide moderate edaphic properties suitable mainly as short-term grazing for animals. The disadvantages, mainly due to the lack of certain nutrients, excessive fluoride and thin, saline soils, make it likely that vegetation growing on soils in these areas would only be exploited by animals for part of the year, with movement elsewhere at other times. At times of high lake levels, fresh water would have been available in the basin but grazing and browsing areas on the rift floor would have been much reduced.
To the east, the Kinangop plateau provides extensive areas of relatively smooth and accessible topography, circumscribed by steep faults or inaccessible areas of rough topography, and moderate nutrient content for most of the tested soils. Lake Ol Bolosat is a fresh water source and the lake shores and associated wetlands provide easy grazing or browse. Mount Kipipiri and the Sattima fault escarpment provide one of the few larger areas of basalt (Sattima basalt). Here, soils tend to be thick and fertile and have very high phosphorus levels in some of the samples tested. In general, most nutrients tested were available in sufficient levels on the soils sampled in this region. The best soils are located in a narrow ring around Mount Kipipiri and a thin strip where the Sattima fault exposes basalt. No soil samples were taken from the Aberdare Range. However, the lithological similarities of the uppermost part of the range to Mount Kipipiri and the thick forest cover suggest thick and fertile soils for this region comparable to Mount Kipipiri.
To the west, the Mau Escarpment presents a significant barrier to east–west movement but there is easy passage from the Nakuru basin through the escarpment to extensive areas of relatively accessible topography at higher altitude, originally covered with dense forest but now extensively cleared for production of tea, coffee and maize, with good soil edaphics.
To the south, the situation is less clear. The Eburru forest today is characterised by a dense forest cover, and thick red, fertile soils with high Ca, Mg, and P levels. However, the onset of volcanism at Eburru is of Holocene age (Bergner et al., 2009; Clarke et al., 1990; Scott & Skilling, 1999) and these high values cannot therefore be extrapolated to earlier times.
When lake levels were high, it is clear that the only feasible pathway for animals to pass along a north–south axis or between the rift floor and the extensive and relatively attractive grazing territory of the Kinangop Plateau would be to cross the Kariandusi River (Figure 5). The distance over which the river can be crossed is in fact only a few hundred metres because of the obstructions on either side. No alternative route is possible. This places the Kariandusi site at a critical point to intersect animals moving along a highly predictable migration route during high lake levels. Conversely, when lake levels were low, at or close to present-day levels, extensive grazing territory would have been available around the lake margin, and the Kariandusi site would have lost its strategic importance, being more easily bypassed.
The combination of edaphic and topographic analysis reveals important features about the palaeoenvironment of the wider region and the location of individual archaeological sites in relation to large-mammal movements that would not otherwise have been apparent. Here, we concentrate on the site of Kariandusi, and consider how far the location of the site can be explained in terms of its unusually advantageous position in relation to the topographic and edaphic variables identified above, as opposed to other factors such as access to water supplies or lithic raw materials, and whether we can infer some form of ‘ambush hunting’ from its location, following the identification of similar combinations of edaphic and topographic features elsewhere, notably at Gesher Banat Yaqov in Israel (Devès et al., 2014), and at Olorgesailie in the southern Kenyan Rift (Kübler et al., 2015).
The Kariandusi site comprises a palimpsest of artefacts, representing an unknown number of depositional episodes (Shipton, 2011). There are two groups of finds, an upper site first excavated by the Leakeys in the 1930s and 1940s on the right bank of a small tributary of the Kariandusi River, and a nearby concentration of stone tools on its left bank excavated by John Gowlett in 1974, with an age bracketed between 0.73 and 0.98 Ma (Gowlett & Crompton, 1994; Shipton, 2011). The material was originally deposited on the river bed or the adjacent banks of the river not far from where it entered an expanded Lake Elmenteita during a period of high lake level. The stone artefacts could have been subsequently re-deposited by river bank erosion though they were probably not moved very far from their original position (Walter & Trauth, 2013), and were later buried in fluvial sediments stratified between underlying lake sediments and overlying lavas. There is no evidence that archaeological or human fossil material was deposited in the nearby lake or lake shore deposits. Some of the archaeological material from both the Leakey and Gowlett excavations has been preserved and protected in situ and is perched on the sides of a more recently formed shallow gorge incised by the Kariandusi River as it cut down to a lowered lake level (Figure 8). The artefact material is dominated by bifaces made of locally available lava, or obsidian possibly obtained from sources up to 30 km to the south on the rift floor and the Kinangop Plateau (Shipton, 2011). Flake debitage is under-represented, suggesting that many bifaces were made elsewhere and discarded at Kariandusi. Faunal remains are very rare, comprising only Equid teeth, most probably all that has survived the effects of post-depositional destruction.
Source material for making artefacts is readily available in the volcanics of the region, and though a lava outcrop is present some 90m to the north, the site has no particular advantage in respect of raw material availability. Similarly, freshwater would have been widely available along river courses, in springs along fault lines, and from an expanded Lake Elmenteita that would have contained freshwater at high lake levels in contrast to the saline conditions that prevail today. Neither of these variables uniquely determines the attractiveness of the Kariandusi location, though they could have been added attractions.
Rather, the key factor is the combination of topographic features further constrained by high lake levels during a limited time window of opportunity that allowed animals to be easily and predictably intercepted. The important features here are the date of the site, which coincides with a period of high lake levels, and the location of the site on the only accessible pathway between the attractive upland soils and topography of the Kinangop Plateau and the resources of the rift floor in the Nakuru-Elmenteita and Baringo basins (Figure 7). If, as is now widely accepted, meat-eating played a significant role in the development and expansion of the Homo lineage (Ben-Dor et al., 2011; Cordain et al., 2000; Aiello & Wheeler, 1995), then availability of such features would have been of critical advantage, providing easy opportunities for hunting or scavenging the meat of large mammals.
This raises two further questions for discussion: what sort of methods of exploiting large mammals are implied by these site locations? And why, in the current state of knowledge, are these sites apparently so rare?
With regard to the first question, ‘ambush hunting’ seems an intuitively obvious interpretation in the circumstances we describe, and we see no reason to deny such abilities to early hominins simply because of their great antiquity (see also Pickering, 2013). However, we note that, when talking about the whole span of human evolution, ‘ambush hunting’ may cover a wide spectrum of possibilities, ranging from high levels of social cooperation and planning at one extreme, involving large groups of people, investment in artificial aids and additional technologies such as the construction of artificial barriers for channelling animal movements, to simpler techniques, at the other extreme, that depend mainly on being in the right place at the right time in a landscape constrained by natural traps that animals are forced to move through during the course of their normal patterns of movement (see Marean 1997, for further discussion). In the absence of evidence at Kariandusi for human population size, details of the material culture, the duration, timing or frequency of individual episodes of activity, or even any direct information about prey animals or evidence from their bone remains, there is a limit to how much we can infer about the social organization, technology and hunting techniques involved other than to highlight the opportunities afforded by the local topography at the time of occupation.
This, in its turn bears on the question of why such sites are not more commonly found. One possibility is that the sites are not rare at all, but are simply a tiny and unrepresentative sample of a much larger distribution of material, most of which has been eroded away, buried under later deposits, or simply has not yet been discovered. In a region of active tectonics, with ongoing volcanic activity and changing lake levels, it is possible that some sites in lake-edge and river-bank locations have been eroded away and buried under later sediments, or have been buried under later volcanic deposits, especially on the floor of the inner rift. On this argument, Kariandusi might be just one of a range of sites involving different patterns of activity and land use, different environmental and topographic associations, different tactics for exploiting animal prey, and quite possibly other facets of economic subsistence involving exploitation of non-mammalian, aquatic or plant resources.
Another possibility is that the surviving pattern of sites has been biased by variations in hominin behaviour with respect to the discard of material. Isaac (1981) was among the first to emphasise the tendency of early African archaeological ‘sites’ to represent clusters or patches of material surrounded by a more widely distributed background scatter of individual artefacts – the ‘scatters and patches’ approach to spatial analysis (see also Isaac & Harris, 1978; Kroll, 1994; Stern, 1994). Isaac further pointed out that the clusters might not be functionally different from the scatters, simply representing the same sort of individual depositional episode repeated many times in the same place – a ‘cumulative palimpsest’ of more recent terminology (Bailey, 2007) – and therefore with a higher probability of achieving a threshold of archaeological visibility. On this argument, there might be more sites scattered across the landscape representing the same sorts of activities as at Kariandusi, but consisting of a single artefact or a small group of artefacts deposited in a given location only once and therefore more likely to have escaped preservation or discovery. According to this hypothesis, any putative differences in visibility of evidence would be the result of pre-depositional variations in hominin behaviour rather than post-depositional variations in exposure or preservation of discarded bones and stones, but the outcome would be the same, namely to compromise any interpretation that sees significance in the relationship between Kariandusi and its local topographic features.
We do not rule out the operation of factors of differential visibility and preservation, but we prefer to look for patterns of association in the evidence that we do have rather than to speculate about the possible meaning of data that may never have existed. We may not be able to say with much confidence precisely what activities were carried out at Kariandusi – hunting, scavenging, sleeping, making tools, caching of raw materials, finding shade and protection in trees, or any of a range of other possibilities, perhaps any or all of these, or different ones at different times. Rather, the significance of Kariandusi lies exactly in the fact that it was the scene of repeated visits and discard of material, and that the main episodes of activity coincide with strikingly advantageous topographic opportunities for the exploitation of large mammals at about the period of time when these opportunities would have been most obviously available.
A final possibility is that sites like Kariandusi are genuinely rare, and that the pattern we see is indeed broadly representative of the distribution of past hominin activities, with their main concentration in widely-spaced locations with unusual combinations of topographic and edaphic features that facilitated easy access to large mammals. Raw material distributions and other features of the artefact assemblage indicate that the makers of the Kariandusi bifaces may have ranged more widely in the area, but that is not inconsistent with a pattern of land use focused on limited and widely spaced nodes of subsistence activity. If correct, this interpretation carries the further implication that hominin populations 1 million years ago were small and concentrated in limited areas of the wider landscape, consistent with recent inferences of small population size from genetic analyses (Sherry et al., 1997; Huff et al., 2010), or that they lacked the skills, motivation or technology to hunt mammals or exploit other food resources more widely in less constrained topography. In this context we note the presence of MSA and LSA material on the Kinangop Plateau and the Mau escarpment in locations that do not seem to have been any less available at earlier periods, and where concentrations of Acheulean bifaces, had they been discarded there, might be expected to have remained just as visible to discovery as the stone artefacts from later periods.
The landscape of the Central Kenya rift is the product of cumulative rifting, tectonic faulting and volcanic activity over a period of more than 5 million years. In this paper we have concentrated on the Nakuru-Elmenteita-Naivasha region. The basic morphology of this region as it appears today had become established by about 2.5 Ma, but ongoing faulting and volcanic activity has continued to transform local features up to the present day, rejuvenating fault scarps and covering some earlier land surfaces with volcanic lavas. Superimposed on these processes are changes in lake level, jointly determined by climate change and tectonic activity. These processes have exerted major controls on the ways in which large mammals were distributed and their accessibility to hominin predation. They have also probably had an impact on the preservation, exposure and discovery of archaeological material, which may account in part for the apparent rarity of sites in this region. No Plio-Pleistocene hominin fossils have yet been discovered, and that may be due to similar factors of preservation, although we note that alkaline lake sediments good for preserving fossil material and formed at higher lake levels are well exposed in parts of the basin, with extensive quarrying below the Kariandusi site, and we might expect fossil material to have been recovered here if it had been available for discovery (Figure 8).
Collecting and analysing nutrients of the soils (soil edaphics) and vegetation provides a key to reconstructing how animals could have used the region prior to the impact of modern agricultural development. Relating this to the mineralogy of the underlying rock (regolith) in a systematic way has not previously been carried out, and the results presented here offer the prospect of producing satellite-based soil and geological maps that can apply to a wider region than the one examined here. The edaphic analysis shows that the distribution of soil nutrients is patchy, with the best conditions on some of the basaltic rocks of the rift flanks and some areas of lake sediment, but with significant deficiencies in many other areas. This feature would have prompted movements of animals in the past and also has important modern social implications because a lack of trace elements has serious consequences for human and animal health today.
Contrary to initial expectations, the rift floor, despite the presence of extensive lakes, is not the most obviously attractive place for human exploitation of mammal-resources. When lake levels were low, the microclimate was generally hot and dry with a short rainy season compared to the rift flanks, and the lakes with small catchments would have become alkaline and unsuitable for drinking water. In wetter climatic intervals with high lake levels, freshwater would have been more widely available in an extended lake region, but the lakes would have flooded extensive areas of previously available animal habitat.
Combining the analysis of topographic and edaphic features has enabled us to produce maps of the region that highlight the areas where hominin predators would have had the best opportunities for targeting large mammals, and a framework for the interpretation of archaeological sites more generally. The site of Kariandusi is especially well placed to capture animals moving between the extensive and attractive upland grazing territories of the Kinangop Plateau to the east and southeast of the site and the Nakuru and Baringo basins to the north and west, especially during periods of high lake level. We interpret the site as an ideal location where simple ambush hunting could have been practised, taking advantage of the natural trap-like features of the local topography in relation to the wider distribution and pattern of movements of large mammals. We cannot rule out the distorting effects of differential preservation and exposure in removing or obscuring archaeological sites elsewhere, but we regard it as significant that the unusual combination of features at the Kariandusi location is associated with the only Acheulean site complex so far discovered in the region, and consider this evidence of some form of ambush hunting. If patterns of Acheulean land use were limited by the availability of natural features like those we have identified at Kariandusi, this might explain the relative rarity of substantial and repeatedly used Acheulean sites in this region and elsewhere, and this has further implications for assessments of hominin population density and hunting skills at this early stage in the hominin evolutionary trajectory.
The research reported here was funded by the European Research Council through ERC Advanced Grant 269586 DISPERSE, under the ‘Ideas’ Specific Programme of FP7, granted to GK and GB in 2011, who undertook a preliminary reconnaissance in the region in 2012 and first formulated the idea for a more detailed research programme of landscape analysis. SK is financially supported by the Helmholtz Alliance EDA. SK, SR, PO and GK formed the core team that devised the protocols for edaphic sampling and collected field samples and observations of vegetation, tectonic features and topography in 2013, with the addition of SCR in 2014. PO conducted the laboratory analysis of the edaphic samples. PO, SK and SR are responsible for the interpretation of the edaphic results, SK and GK for the tectonic interpretation of the landscape, GK and SCR for the interpretation of animal movements, and GB for the archaeological interpretation and discussion. We are indebted to our sponsors in the field, the Kenyan National Commission for Science, Technology and Innovation, the National Museums of Kenya, the Kenya Agricultural and Livestock Organization, and the British Institute in Eastern Africa for the provision of permits, support and facilities. We also thank Dr Inmaculada Lopez of the Institut de Physique du Globe, Paris for discussions and great help with DISPERSE project logistics, Purity Kiura of the National Museums of Kenya for encouragement and facilitating contacts and logistics in the field, Karega Munene for hospitality and help in Nairobi, and Kenneth Risjdijk and an anonymous reviewer for helping us to improve the clarity of the text. This is DISPERSE contribution number 30 and IPGP contribution number 3764. We dedicate this paper to the memory of Peter Owenga, who played a key role in the edaphic analysis, but who died in 2015 before he could see the full realization of his contribution.
The authors declare that they have no competing interests.
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