Past and Present at Wonderwerk Cave (Northern Cape Province, South Africa)
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The Northern Cape Province and neighboring North West Province (Bokone Bophirima) of South Africa provided the first scientific evidence for the centrality of Africa for hominin evolution. In the late 1800s, long before the fossil hominin finds at Olduvai Gorge in East Africa or the Cradle of Humankind sites in Gauteng Province, alluvial diamond diggers found extensive assemblages of Earlier Stone Age (ESA) artefacts in the Vaal River gravels at localities such as Klipdrift (Canteen Kopje) in the Northern Cape (Johnson and Young 1906). World-famous prehistorians visited the area and described the archaeological findings (e.g., Péringuey 1911; Goodwin 1928; Goodwin and van Riet Lowe 1929; Breuil 1945; Mitchell 1998; Kunneriath and Gaillard 2010). Despite the extraordinary discovery of the Taung Australopithicine skull in 1924 at a quarry located ca. 120 km to the northeast of the Vaal gravel localities (Dart 1925), in the following years, this region was largely overlooked by the scientific community. This was due to the fact that the Taung skull had no clear archaeological context, while confusion sown by the “Piltdown Man” and resulting debates surrounding what constituted the “missing link” occupied primary place in discussions within the anthropological community (Tobias 1992). The spectacular fossil hominin finds in East Africa and Gauteng from the 1940s onwards further shifted the spotlight away from the Northern Cape, even though numerous paleontological and archaeological investigations of the Pleistocene and Pliocene continued in this region (e.g., Malan and Cooke 1941; Camp 1948; Peabody 1954; Power 1955; Wells 1964; Sampson 1974; Butzer et al. 1978).
Wonderwerk is located along the route that led from the Vaal River to the Moffat Mission in Kuruman, and it is likely that the site was visited frequently by early travelers in the region. As shown in Fig. 1, a cave that likely corresponds to Wonderwerk is indicated on a map published in 1844. This map shows clearly that, in the years preceding the diamond rush, the Kuruman Hills were relatively well travelled primarily due to the presence of the Moffat Mission. The cave is described in publications of European travelers, for example, James Backhouse (1844), who visited the region in 1839 but did not visit the cave himself, and Methuen (1846), who did enter the cave in 1844.
Studying the excavated and as yet unstudied finds (lithic, faunal and botanical) from the Beaumont and Thackeray excavations;
Contextualizing these finds in terms of their geological and chronological settings;
Examining the association of the different finds within and between strata;
Directly dating the ESA levels using a range of chronometric methods as well as filling gaps in the Holocene dating sequence;
Reconstructing the palaeoenvironmental and palaeoclimatic conditions that prevailed around the site and in the region as a whole over the entire chronological sequence;
Undertaking fine resolution excavation to clarify stratigraphic associations and the nature of the cave occupations, and
Publishing all finds from past excavations in the cave as well as from current ones.
Recognition of the archaeological significance of Wonderwerk Cave has been a gradual process. To date, several papers resulting from this new project have been published (e.g., Avery 2007; Brook et al. 2010; Berna et al. 2012; Chazan and Horwitz 2009, 2015; Chazan et al. 2008, 2012; Matmon et al. 2012; Brink et al. 2015; see project website http://www.wonderwerkcave.com), and numerous papers and posters presented at international conferences. A particularly significant milestone was the creation of a 3D model of the cave by the Zamani Project (Rüther et al. 2009). The ten papers in this special issue of African Archaeological Review, along with three forthcoming papers to be published in a subsequent issue of this journal in 2016, provide a further and especially valuable contribution, since they afford the first in-depth overview of central aspects of this important archaeological locality. The papers focus on Pleistocene and Holocene material from the front of the cave, primarily from Excavation 1, located immediately behind a large stalagmite situated ca. 20 m in from the cave entrance (Fig. 2).
Stratigraphy and Dating
Peter Beaumont collaborated with J.C. Vogel to develop a radiocarbon chronology for the LSA levels at Wonderwerk, and both A. and F.J. Thackeray pursued similar analytical work (for a summary of all their 14C dates, see Lee-Thorp and Ecker 2015, this issue; Scott and Thackeray 2015, this issue). Though the quantity and caliber of the 14C dates were excellent, they were never calibrated or modeled to create a robust chronostratigraphic framework. This work has now been undertaken by Scott and Thackeray, as well as Lee-Thorp and Ecker, and is presented in this issue. The calibrated 14C series using Bayesian models provides new insights into the LSA chronology: (i) four previously unpublished dates were added, (ii) the calibration and modeling produced a longer sequence than previously reported based on radiocarbon years alone and now spans some 15,000 years, and (iii) the model provides greater accuracy for the timespan of the occupation of each stratum. This new analysis provides an excellent basis for understanding the extensive Holocene sequence in Excavation 1.
The Earlier Stone Age archaeology in southern Africa has long been limited by the absence of reliable dating methods. Beaumont and Vogel (2006) employed U/Th dating of speleothems to extend the chronology of the cave into the Pleistocene and also reported the findings of the paleomagnetic analysis undertaken by K. L. Verosub of Excavation 1 (Beaumont and Vogel 2006: Tables 2 and 3). Unfortunately, these results are incompletely presented and so of limited value in providing a comprehensive chronological framework for the ESA in Excavation 1.
Developing a robust chronometric framework for the Earlier Stone Age deposits at Wonderwerk was one of the key goals of our renewed research project. The principles underlying this research have been the application of multiple methods, and the importance of understanding the geological contexts of the samples used for dating. Dating specialists are involved in fieldwork and take samples themselves whenever possible.
For the ESA, the most productive methodology for Wonderwerk Cave has been the pairing of paleomagnetism and cosmogenic burial age dating, which are independent systems that both rely on a thorough understanding of geomorphology. The paper in this issue by Goldberg et al. provides the critical geological context for the dating program based on a combination of field observations, micromorphology, and FTIR analysis. At a broader scale, Matmon et al. (2012) provide grain size analysis that demonstrates that the Kalahari was the primary source for the sands found in the Wonderwerk infill.
Paleomagnetic dating determines the direction of the earth’s magnetic field when sediments were deposited. A paleomagnetic sequence can be correlated with the global magnetic sequence; however, it is essential that there is an anchor that places the signal in the global curve. In Wonderwerk Excavation 1, the paleomagnetic analyses have identified a sequence of Normal > Reverse > Normal (Chazan et al. 2008; Matmon et al. 2012). To anchor this sequence, we turned to cosmogenic burial age dating (Matmon et al. 2012). This method determines the time that has elapsed since sediment has been shielded from cosmogenic radiation using the ratio of cosmogenic isotopes 26Al /10Be, which have different decay rates. The burial history of sediments prior to their entry into the cave complicates the interpretation of isotope ratios and it is important to keep in mind that the results obtained tell us when the sediments first entered the cave rather than the timing of their final deposition.
The extensive cosmogenic sequence in Excavation 1 permits us not only to anchor the paleomagnetic sequence, but in some cases to also further constrain the age of deposits. The lower normal (in stratum 12) is bracketed by ages that situate it in the Olduvai event, while the upper normal (strata 10 and 9) is bracketed by cosmogenic burial age dating consistent with the Jaramillo subchron, a brief event of only 100 kyr. It is important to emphasize that the paleomagnetic and cosmogenic ages are in complete agreement on the age of this sequence. Unfortunately, the intervening reversal (top of stratum 12, stratum 11, and bottom of stratum 10) is a very long period and further cosmogenic age determinations are needed to further constrain the age of deposition within this time period. The uppermost part of the ESA sequence (strata 8–6) is not yet constrained by cosmogenic burial ages, and for the upper part of stratum 9, only paleomagnetic dating is available. All of stratum 9 was deposited during conditions of normal polarity. However, for the upper part of the stratum, where we currently lack cosmogenic ages, we cannot rule out the possibility that it was deposited during the Jaramillo subchron and not the Bruhnes chron. If this scenario is correct, this would require the presence of a major unconformity within Stratum 9.
Dating ESA deposits at Wonderwerk Cave using OSL (including TT-OSL) have been unsuccessful (Chazan et al. 2008; Naomi Porat, pers. comm.), but this method will doubtless be of great value for dating the MSA and even LSA strata. Pickering (2015, this issue) describes U/Pb dating of small speleothem straws that have produced meaningful results. However, the significance of these results for Wonderwerk Cave are limited, to some extent, by the imprecise nature of provenance data for material from Beaumont’s excavation (for details on provenance problems, see papers in this issue by Chazan, and Birkenfeld et al.). U/Pb dating will, however, have potential to make a major contribution in the context of the renewed excavations.
The current project has, as yet, not undertaken extensive dating of the other excavation areas within the cave. One exception is Excavation 6 at the back of the cave for which both the paleomagnetic and cosmogenic burial dating sequences have been published (Matmon et al. 2012). Work is currently underway to date the sequence in Excavation 2 (e.g., Pickering 2015, this issue), which includes an MSA component.
Pleistocene archaeological deposits are found in three areas of the cave (Fig. 2): Excavation 1 (front of cave behind a large stalagmite), Excavation 2 (behind and offset immediately to the right of Excavation 1), and Excavation 6 (located in the very back of the cave, 140 m in from the entrance). Excavation 6 has produced a remarkable assemblage attributed to the Fauresmith associated with quartz crystals, modified ochre, and specularite (Chazan and Horwitz 2009; Chazan 2015a; Watts et al. 2015). In Excavation 2, a sequence that includes ESA and MSA components was documented (Beaumont and Vogel 2006). The detailed analysis of these collections is still in process, but the attribution of stratum 2 in Excavation 2 to the MSA, as proposed by Beaumont, is secure.
In Excavation 1, the ESA sequence (strata 12 through 6) is truncated by stratum 5 and is immediately overlain by four LSA strata (strata 4 through 1), subdivided in places into sub-units (a-d). The LSA lithic sequence has previously been described by A. Thackeray (Humphreys and Thackeray 1983). It comprises an Oakhurst industry, locally designated as the Kuruman Industry, in stratum 4d (with a boundary age of 12,900–9,000 cal. bp; Lee-Thorp and Ecker 2015, this issue) dominated by scrapers, with banded ironstone and dolomite used as raw materials. It is overlain by a Wilton industry (in strata 4b-c) characterized by scrapers on banded ironstone (5,500–9,800 cal bp). A marked shift in artefact types and raw material is evident at the top of level 4b. The overlying Wilton industry, in strata 4a to 3b, contains backed bladelets on chert (5,800–2,300 cal. bp) finally topped by a ceramic LSA in strata 2b-3a (900–2,800 cal bp) and historic period material (disturbed contexts) in strata 1–2. The nature of stratum 5, which is characterized by subrounded dolomite clasts and both ESA and LSA lithic material, is the subject of ongoing investigation (e.g., Bamford 2015a, b, this issue; Lee-Thorp and Ecker 2015, this issue; Scott and Thackeray 2015, this issue).
The rock art adorning the first 40 m of the cave walls is a rare example of painting in a region where rock engravings, but not paintings, are widespread. The rock art includes a wide diversity, both thematically and stylistically, of animals and geometric forms. In a forthcoming article, Morris (2015) presents the first extensive discussion of this important corpus. One of the great challenges for site management at Wonderwerk is providing for the long-term preservation of the paintings while allowing for visitor access. A graffiti-removal project undertaken in 1993 by S. Bassett and J. Deacon was intended to provide a remedy for the extensive historical graffiti that largely obscured the cave paintings. Unfortunately, this intervention, which included infilling and overpainting, has not weathered well, leading to additional conservation challenges. Wonderwerk is also well known for the decorated stone slabs recovered during excavation in the LSA strata, which were the earliest securely dated art in Africa long before the dramatic discoveries at Blombos Cave (Thackeray et al. 1981; Beaumont and Vogel 1989). Thackeray and colleagues (Thackeray 2005; Bradfield et al. 2014) have recently returned to the interpretation of the images found on these slabs.
The ESA of Excavation 1 provides a unique opportunity to track the development of Acheulean lithic technology over time. It is important to emphasize that the Oldowan/ESA lithics in Excavation 1 occur in low densities. The paper by Chazan in this issue provides the first extensive technological analysis of this assemblage. The timing and nature of technological changes in the Acheulean at Wonderwerk fit well with what is known in East Africa, despite limitations in chronological resolution for the early stages at Wonderwerk Cave.
An important discovery resulting from the renewed investigations at the site has been the presence of an Oldowan industry in stratum 12, at the base of Excavation 1, that is characterized by small tools including flakes and cores. The absence of large choppers, cleavers, and spheroids in the Wonderwerk Oldowan might be a result of the small sample size. The presence of a small flake component fits well with what is known of the Oldowan from the South African sites of Sterkfontein and Swartkrans (Granger et al. 2015) and several East African sites (see discussion and references in Chazan et al. 2012). The cultural attribution of this industry at Wonderwerk is supported both by the chronometric ages for this layer and the biochronology of the macrofauna, which contains archaic elements including two extinct species of hyrax (Procavia), and an extinct large caprine (Brink et al. 2015, forthcoming). Thus, the faunal taxa associated with the Wonderwerk Oldowan assemblage share common features with other sites dating to the Makapanian Land Mammal stage, such as Makapan Limeworks Member 3 (Reed 1996), Swartkrans Members 1 and 2 (De Ruiter 2003; Watson 2004), and Sterkfontein Member 5 (Ogola 2009).
The in situ nature of the Oldowan deposit has been demonstrated by the micromorphological analysis of the sediments, further supported by the distance of the excavated material from the current cave mouth and absence of alternative entrances. These findings make the stratum 12 deposit at Wonderwerk the earliest evidence for intentional cave occupation worldwide (Chazan et al. 2012; Goldberg et al. 2015, this issue).
During his excavations, Beaumont recorded provenience of finds in 10 cm spits within 1 yard-square units. Consequently, there are limits to the precision of the spatial data from his excavations, and the absence of detailed field notes and photographs makes correlation between archaeological strata and depositional events even more problematic. However, the spatial data available do allow exploration of association between classes of material recovered and the spatial organization of activity within strata. To overcome this drawback, Birkenfeld et al. (2015, this issue) have used GIS to create virtual reconstructions of spatial and temporal distributions of finds from excavation 1, despite the absence of piece-plotted data. The virtual excavation grid they created acts like a cupboard, in whose drawers (excavated squares) the different finds are placed in virtual space based on their square number, stratum attribution, and depth data. The authors were able to test both the vertical and horizontal dispersal of macro- and microfaunal remains from the Oldowan/ESA levels. This innovative study holds great promise for analysis of patterning in the “old collections” from the cave, while given that all finds from the new excavation are geo-referenced, results of spatial analyses based on the old assemblages can be verified in the future.
Evidence for Use of Fire
Based on macroscopic observations, Beaumont (2011) identified potential evidence for the use of fire at Wonderwerk as far back as stratum 12. In a publication from the following year, Berna et al. (2012) provided the earliest, well-contextualized evidence for the use of fire by hominins ca. 1.0 Ma years ago, based on the identification of wood ash in micromorphology slides from stratum 10 in Excavation 1, dated to the Jaramillo subchron. This initial observation is supported by FTIR analysis of bones from this layer that show evidence of burning and potlid fractures on lithic material. Potlid fractures have now been observed on artifacts recovered in situ in the renewed excavations of stratum 10, providing corroboration for this finding.
Several papers in this issue bring new perspectives to our understanding of the use of fire at Wonderwerk. Goldberg et al. (2015, this issue) examine the evidence for fire in stratum 10 and point to the need for caution when identifying ash in micromorphological slides from this layer, given the co-occurrence of rhizoliths that have a similar morphology to burnt ash. Chazan et al. (2012) have presented evidence for burnt micro- and macrofauna in the Oldowan assemblage from stratum 10, while the current papers by Fernandez-Jalvo and Avery (2015, this issue) and Brink et al. (forthcoming) provide further evidence for burnt fauna and microfauna in the underlying strata 11 and 12. Fernandez-Jalvo and Avery (2015, this issue) report a high proportion of micromammalian remains with evidence of burning, including calcined bones. Moreover, the burnt bones appeared to be in concentrations. The authors note that both traits do not fit with natural fires. According to Brink et al., the fact that a large proportion of the macromammalian remains in these layers was burnt may have contributed to the extensive fragmentation to both bones and teeth in this assemblage. Bamford (2015b, this issue) reported one piece of charcoal from stratum 12, while no large charcoal fragments were recovered from stratum 10 (Berna et al. 2012). Calcified roots and plant litter from stratum 10 were tentatively interpreted as kindling (Berna et al. 2012). The caliber of the observations for intentional use of fire in stratum 12, then, differs from that available from stratum 10 where burnt material could be identified in context on preserved surfaces through the use of micromorphology. It is unlikely that such a level of resolution will be found for stratum 12, as the sediments that compose these strata were deposited by low energy, sheet-water flow and as such do not preserve intact surfaces. Thus, the nature and significance of the evidence for fire in the Oldowan of Wonderwerk Cave require further investigation, though it seems beyond question that fire (intentionally or accidentally) was present in the cave as early as the Oldowan occupation, at least 1.5 Ma years ago.
Palaeoenvironmental and Palaeoclimatic Evidence
One of the major contributions that renewed research at Wonderwerk Cave can make to the archaeological record of southern Africa lies in the study of past environments and climatic conditions. This stems from the dearth of suitable datasets from the interior of southern Africa that can serve as climatic proxies. The excellent preservation of organic remains at the cave, the presence of a robust chronometric framework, and the association with a long cultural record makes this a rare archive.
Late Pleistocene and Holocene
The contribution here by Brook et al. supplies the first dates for tufa deposits located immediately outside and just inside the current cave entrance. All are younger than ca. 3000 cal year bp, providing an important corroboration that in the past they formed under more protected conditions, when the cave entrance was located further forward, but subsequently receded since the early Pleistocene as initially proposed by Matmon et al. (2012).
Examination of a core extracted from the stalagmite adjacent to Excavation 1 provided information on moisture penetration into the cave and hence palaeoclimatic conditions in the region (Brook et al. 2010). Evidence for growth of the speleothem implies that conditions were moist enough for water to penetrate the epikarst, while a hiatus represents periods when this did not happen, presumably because there was not enough moisture penetration. Based on this core, moist and cool conditions were reported for the Late Pleistocene at ca. 35,000–33,000 cal year bp and ca. 22,000–14,000 cal year bp with brief, dry episodes at ca. 34,000 cal year bp, ca. 22, 000 cal year bp, and ca. 15,000 cal year bp (Brook et al. 2010). Pollen recovered from inside this stalagmite core also provides palaeoclimatic indications. Overall temperatures were cool as suggested by a fynbos component with a brief interlude ca. 16, 000–14,000 cal year bp when pollen suggests that temperatures increased, before returning to cooler conditions equivalent to the Younger Dryas event. This coincides with a growth hiatus in the large stalagmite between ca. 13,300 and 3500 cal year bp (Brook et al. 2015, this issue). Parts of this hiatus are represented by pollen in dung deposits, and excavated floor deposits, indicative of cool conditions up to ca. 12,500 cal year bp. Bamford (2015a, b, this issue) also reports slightly more mesic conditions in Late Pleistocene stratum 5 (>12,000 bp: Lee-Thorp and Ecker 2015, this issue) than those prevailing around the cave today. The markedly lower δ13C and δ18O isotopic values for ostrich eggshell samples from the same stratum 5 are indicative of a large C3 plant component during this phase, interpreted as likely due to higher moisture and lower growth season temperatures (Lee-Thorp and Ecker 2015, this issue). The phase between ca. 12,000 and 6000 cal year bp pollen shows high frequencies of Asteraceae (Scott and Thackeray 2015, this issue), suggesting large proportions of C3 vegetation, consistent with the OES carbon isotopic composition (Lee-Thorp and Ecker 2015, this issue). Based on pollen, isotopes, and microfauna, conditions were generally dry, but there are some indications that moisture availability fluctuated to reach subhumid conditions, e.g., ca. 11,000 cal year bp.
Data on macromammals (Thackeray 1983, 1984, 2015, this issue) and previously published data on micromammals (Avery 1981, 1995) from the Holocene layers at the cave have been interpreted as indicating generally moister conditions in the Early Holocene from ca. 7500 to 5100 year bp. This partly overlaps with the time range of moist conditions prevailing in the mid-Holocene from ca. 6100 to 5300 year bp as proposed by Lee-Thorp and Ecker (2015, this issue). Thereafter, there was a shift to more arid conditions. Likewise, the pollen data suggest a change in the mid-Holocene from moist grassy conditions ca. 5500 year bp, that consequently became slightly drier to support veld similar to that in the cave’s environs today (Scott and Thackeray 2015, this issue). This change has tentatively been attributed to reduced winter rainfall and a concomitant increase in summer precipitation (Lee-Thorp and Ecker 2015, this issue).
Isotope data show that the trend towards aridification culminated at about 2000 years, which is consistent with pollen data, indicating a slightly drier grassy vegetation at this time (Scott and Thackeray 2015, this issue). An increase in grazers (as reflected in higher numbers of springbok, Antidorcas marsupialis), in parallel, reflects the expansion of grassland environments (Thackeray 2015, this issue). Further evidence for the “2–3 ka dry period” was found in both the tufa and stalagmite, highlighting that this event may have impacted large parts of the summer rainfall zone of southern Africa (Brook et al. 2015, this issue). After this, conditions fluctuated with several dry intervals at 0–80, 250–400, 550–750, 1200–1500, 2100–2250 cal year bp, interspersed with moist intervals at 80–250, 400–550, 750–1200, 1500–2100, 2250–2500 cal year bp. Pollen data derived from the stalagmite indicate similar shifts though with less chronological resolution: dry and cool conditions from ca. 1540 to 740 cal year bp followed by warmer and moister ones from ca. 740 cal bp to today (Brook et al. 2015, this issue).
In their paper, Fernandez-Jalvo and Avery describe and discuss the taphonomy of the micromammalian remains from the Oldowan/ESA layers, strata 12 and 11, and report that most of the damage is consistent with that resulting from a raptor, probably the barn owl (Tyto alba). They also relate that at least two concentrations of bones indicative of roosts could be identified, a finding which is independently corroborated by the GIS analysis undertaken by Birkenfeld et al. (2015, this issue). Fernandez-Jalvo and Avery (2015, this issue) also suggest that the high frequencies of Gerbillinae and Chrysochloridae in stratum 12 may reflect a relatively drier and more open environment compared to the overlying stratum 11 with higher frequencies of Soricidae, characteristic of moister and cooler conditions.
The Oldowan/ESA strata yielded only a few macrobotanical remains, and so do not offer clear insights of the past vegetation cover (Bamford 2015b, this issue). However, their very presence implies that with an excavation protocol aimed at retrieving such delicate remains (slow and very careful excavation, extensive flotation of sediments, etc.), it may be possible to increase the size of the botanical assemblage substantially.
In contrast, the papers by Rossouw (forthcoming) and Brink et al. (forthcoming) offer extensive information concerning the early Pleistocene palaeoenvironmental record of Wonderwerk Cave. Brink et al. provide data on macromammals only for strata 12 and 11. Bovids characteristic of semiarid conditions make up the bulk of the mammalian faunal assemblage. Despite the small sample sizes, a shift between stratum 12 with more alcelaphines and fewer equids to the opposite proportions in stratum 11 may reflect a change from drier to moister (cooler) conditions, supporting that observed in the micro-mammal assemblages.
Rossouw’s forthcoming paper offers a comprehensive record of phytolith assemblages from strata 12 through 9 in Excavation 1. Phytolith composition at the bottom of stratum 12 (dated to ca. 1.96 Ma) correlates with a warm Savanna to Nama-Karoo C4 grassland. This develops into a drier and cooler environment by the top of stratum 12 (dated to ca. 1.78 Ma) and continues through to the base of stratum 10 (dated to ca. 1.07 Ma). Based on modern morphotype ecology, this drier and cooler environment would be analogous to a Succulent Karoo community and characterized by C3 subfamilies. The succulent Karoo biome presently lies more than 1000 km from the cave on the Atlantic coast (Fig. 2). Its shift eastwards to the environs of Wonderwerk Cave would have been facilitated by moister and cooler conditions, possibly resulting from the encroachment of the winter rainfall regime. Further evidence for moist climatic conditions in the region at this time may be the presence of a shallow body of water dating to ca. 1.2–1.0 Ma, at Mamatwan located ca. 80 km north of Wonderwerk Cave (Fig. 1; Matmon et al. 2015). By 1.0 Ma, this body of water had dried up. According to the phytolith record, in mid-stratum 10 (dated to ca. 1.0 Ma), extreme fluctuations are evident from cooler to warmer conditions, with a general shift back to a warm Savanna to Nama-Karoo C4 grassland by stratum 9. Stable isotope ratios measured on fragments of OES from the same Oldowan/ESA strata chart a similar palaeoenvironmental shift as that recorded by the phytoliths, including fluctuating vegetation signals in stratum 10 (Ecker et al. 2015).
The papers in the issue represent a step forward in making the results of scientific research at Wonderwerk Cave broadly available. They highlight new finds and insights regarding chronology, material culture, cave occupation history, and palaeoenvironmental and palaeoclimatic conditions at the site and in its surrounds that have far-reaching implications for our understanding of the prehistory of the arid interior of southern Africa as a whole.
Research continues on the wealth of evidence recovered from previous excavations at the site, and a new phase of excavation has now begun aimed at improving recovery of finds and their in situ documentation. The scientific research is integrated with ongoing efforts led by the McGregor Museum and aided by the South African Heritage Resources Agency to protect this spectacular site and make it accessible to the general public. The studies presented here make the importance of Wonderwerk Cave apparent and also leave us well aware that in this context we have truly only scraped the surface.
We would like to extend our warm thanks to: all members of the Wonderwerk Cave team for their enthusiastic and dedicated support of the project; Colin Fortune (ex-Director), Leon Jacobsen (ex-Vice-Director), Sunet Swanepoel (current Director), and Dr. David Morris (Head of the Archaeology Department) of the McGregor Museum for their support of all aspects of our research project; students from University of Toronto, Simon Fraser University, and other academic institutions who have assisted in field work over the years; Neels Lehule, Iris Khabae, and Johhny Esau, the past and present custodians at the cave, for their help during field seasons. We are grateful to Heinz Rüther and the team from the Zamani Project who, along with Steven James Walker, have provided support for mapping in the cave and the surrounding area, to Jacqueline Studer for translating most of the special issue’s abstracts into French, and to Louis Scott, George Brook, and Julia Lee-Thorp for comments on an earlier draft of parts of this manuscript. We would like to acknowledge the invaluable contribution of our friend and colleague the late Hagai Ron, who undertook the paleomagnetic analysis of Wonderwerk Cave, and to whom this special issue is dedicated. Fieldwork at the site is carried out under permit issued by the South African Heritage Resources Agency (SAHRA) and analysis of the archaeological assemblages under the terms of a signed agreement between MC and the McGregor Museum. The current research program builds on the earlier work of Peter Beaumont at the site. Research at Wonderwerk Cave has been funded over the years by grants to MC from the Canadian Social Sciences and Humanities Research Council, Wenner-Gren Foundation and the Halbert Academic Exchange Fund, University of Toronto. We are particularly grateful to Adria LaViolette for the opportunity to publish this issue and for the editorial guidance she has provided.
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