GEOARCHAEOLOGY AND PREHISTORIC ...

GEOARCHAEOLOGY AND PREHISTORIC TRANSITIONS IN THE AZRAQ Druz BASIN, JORDAN: PRELIMINARY DATA AND HYPOTHESIS FOR A 4-DIMENSIONAL MODEL OF LANDSCAPE CHANGE Christopher J.H. Ames and Carlos E. Cordova

Introduction The Azraq Basin in eastern Jordan has long been the focus of archaeological research, producing a record of occupation from the Lower Palaeolithic to historical periods (Copeland and Hours 1988; Cordova et al. 2008; Cordova et al. 2009; Garrard et al. 1985, 1986, 1987, 1988, 1994; Richter 2009; Rollefson et al. 1997; see Nowell's and Bisson's chapters in this volume). Additionally, the Azraq Basin is positioned between the areas of influence of the Mediterranean Sea and Indian Ocean, making it highly sensitive to global climatic fluctuations and thus an ideal location for paleoclimatic investigations (Abed et al. 2008; Bar-Matthews et al. 2003; Macumber 2001; Turner and Makhlouf 2005). The rich archaeological record in Azraq is often attributed to the local springs, which would have provided resource refugia for prehistoric populations, continuing to support flora and fauna even during periods of dry, harsh conditions (Copeland 1988; Henry 1986; Macumber 2001 ). Such an attractive locus of human occupation, set in a dynamic environment, and spanning critical periods of our species' evolution, makes the Azraq basin an ideal location to study the complex evolutionary relationship between hominins (Homo erectus, H. neanderthalensis and H. sapiens) and environmental change. The Azraq Basin is situated approximately 80 km to the east of Amman and is a major crossroad for travel between Amman, Saudi Arabia, and Iraq (Fig. lA). This endorheic basin is fed by wadis originating in Jordan, southem Syria, and northern Saudi Arabia, which all drain into the bottom of the depression known

as Qa'Azraq. Many publications have described the geographical and geological setting and they will not be described in detail here (see Copeland 1988; Copeland and Hours 1988; Garrard et al. 1985, 1986, 1987, 1988, 1994; Ibrahim 1996; Richter 2009; Richter et al. 2008). The majority of archaeological work in the Azraq region has focused on the northwestern part of the basin, which is divided into a northem and southern area, both situated near historic springs and marshlands on the western and northwest edge of the Qa'Azraq (Fig. lB). The North Azraq settlement, nearest the former Druz Marsh, has been dry since the late 1980s due to a lowering of the water table as a result of overpumping the aquifer (Abed et al. 2008). The South Azraq settlement is located near the Azraq Wetland Reserve, which is managed by the Royal Society for the Conservation of Nature (RSCN). The current wetland in the reserve was restored by pumping water in from one of the wells. The wetland, however, occupies only a minimal area (roughly 7%) of the original wet area. Prior to the reduction in the water table, the North Azraq Basin was a highly dynamic seasonal hydrological system characterized by seasonal changes in the quality and amount of water in the marshes due to spring flow and fluvial input (Nelson 1973; United Nations Development Programme 1966). The system of seasonal water flow involved exchanges of water between the marshes and the Qa' Azraq (Fig. 2). At the onset of the rainy season, or winter, when the water levels were still low, the wadis flowed into the centre of the Qa'Azraq. The level of the seasonal pond would force wa-69-

C.J.H. Ames et al.: Geoarchaeology and Prehistoric Transitions in the Azraq Druze

Jordan s Prehistory: Past and Future Research

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The intensive survey of the Arzaq Basin led by Andrew Garrard in the 1980s (Garrard et al. 1985, 1986, 1987, 1988, 1994) recognized numerous stratigraphic features suggestive ofwetter environments during the late Upper Palaeolithic and early or mid-Epipaleolithic (Garrard et al. 1987: 22). Recent excavation at Kharaneh IV and work at sites within the RSCN wetland reserve are also actively examining the paleoenvironments of Azraq that span the last glacial-interglacial transition (Richter 2009; Richter et al. 2008; Rollefson et al. 1997). Furthermore, using geomorphology and global climate data (Turner and Makhlouf 2005), as well as locally identified upland deposits of Cardium shells (Abed et al. 2008), it has been postulated that the Azraq region contained a large Pleistocene lake(s). Our recent work in North Azraq, in and around the former Druz Marsh (Figs. 1 and 3), substantiates these suggestions and has identified a complex stratigraphic succession characterized by cyclical aggradations of lacustrine and/or palustrine facies indicative of wet periods, intercalated with erosional unconformities and pedogenic carbonate formation suggestive of drier environments. Coupled with the substantial evidence of upland paleoshorelines in the basalt flows that flank North Azraq, we hypothesize that during the past 350,000 years the Azraq region and local populations experienced dramatic environmental fluctuations, at least three distinct pa-

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Summary of Field-Work The stratigraphic profiles and geomorphological descriptions presented here were recorded during our 2008 and 2009 field seasons in North Azraq, particularly in the Druz Marsh (Fig. 1, see Nowell this volume). Until now, very little archaeological material has been reported from the Druz Marsh because it was under water until the late 1980s. However, the marsh is now completely dry and construction is encroaching upon the recently exposed marsh bed. It is this scenario to which we arrived in June of 2008. Construction crews had opened three large pits related to the installation of toilet facilities, a septic system, and water storage at the new Azraq Cultural Centre and Children's Park (Fig. 3). We were granted permission to examine the pits, which we subsequently named DM-1, DMlX, and DM-lY (see location on Fig. 3). Due to time limitations however, we were only able to examine DM-1 in detail. During this salvage project we encountered a complex stratigraphic succession containing abundant Kebaran and Lower Palaeolithic type lithic material. Consequently, we obtained permission to continue investigating the adjacent land, opening five 1x1m hand-dug test pits

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or sabkha (Abed et al. 2008). However, previous archaeological and geomorphological studies have shown that this historical system may have behaved differently or been acting on a larger scale during the Quaternary (Abed et al. 2008; Copeland 1988; Copeland and Hours 1988; Frumkin et al. 2008; Garrard et al. 1985, 1986, 1987, 1988, 1994; Macumber 2001; Richter 2009; Richter et al. 2008; Rollefson et al. 1997; Turner and Makhlouf2005).

ter to flow through channels toward the marshes where it would mix with the wetland. By the end of the rainy season the flow from the marsh would equal the flow from the Qa' itself, recharging the springs for the dry season. During the dry season, or summer, the fluvial influx from the wadis to the Qa' stopped, but the recharged springs maintained a strong flow into the basin, where water would quickly evaporate under high temperatures leaving a salt mudflat

leoenvironments, including large perennial lakes we suspect occurred during MIS 9, MIS 7, and MIS 5.

3. Detailed map of field work locations in the former bed of the Druze Marsh, note the location of Azraq Castle for comparison with Figure 1. -71-

s

C.J.H. Ames et al.: Geoarchaeology and Prehistoric Transitions in the Azraq Druze

Jordan Prehistory: Past and Future Research ent our hypothesized model for the past 350,000 years of fluctuating water levels. We conclude with an outline of our prospective research.

(DM-2 to DM-6) and three 3x1.5m geological · trenches (DM-7, DM-8, DM-9) (Fig. 4). We also conducted archaeological and geoarchaeological survey in and around Wadi al-'Unqiyya to the north (Fig. 1, see Bisson this volume). Near the end of the 2008 field season, during restorative work on the southwest foundations of the Azraq Castle, workmen encountered in situ Middle Palaeolithic (MP) artifacts. We returned to the Druz Marsh for the 2009 field season and undertook a controlled 2x1m excavation adjacent to the southern wall ofDM-8. We also documented two additional stratigraphic profiles (DM-10 and DM-11) situated near the eastern side of the current road, in between the Azraq Castle and the suite of DM profiles recorded in 2008. Survey of the upland basalt flows identified considerable evidence of eroded paleoshorelines surrounding the northern and western perimeters of the former marsh (Figs. 6 and 7) and a test excavation was conducted behind the Azraq Castle but we were unable to locate the MP deposits encountered in 2008. The remainder of this paper discusses the results of this field work in two sections. First, we look in detail at the stratigraphic evidence for fluctuating environments in a suite of documented profiles and, second, we incorporate this information into the North Azraq landscape and pres-

Stratigraphy At present we have documented 12 stratigraphic profiles in detail and traced the succession of facies horizontally throughout the marsh. The stratigraphic relation connecting ten of these profiles (Fig. 4) corresponds to topographic profile 3 (Fig. 3). To contextualize the stratigraph; we provide a detailed description from DM-8 (Fig. 5) and then discuss pertinent variations that appear in other profiles throughout the former marsh bed.

Section DM-8 The top 3 units (6, 5 and 4b) are late Holocene. They contain a mixture of Neolithic and Epipaleolithic lithic material, and Byzantine pottery. Unit 6 is a calcified deposit associated with evaporation of the historic marsh and Unit 5 is an organic soil that was permanently saturated with water, perhaps the waterlogged organic sediment of the historic marsh. Unit 4b is a channel fill, probably laid by a mudflow produced by torrential rain. Unit 3e is a black clay deposit, which seems to be produced by an organic-rich lake environment. Carbonates are present in the top of this

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between the green clay stratigraphic units, the level of the historic marsh, and the surveyed paleoshorelines eroded into the upland basalts. Both topographic profiles 3 and 4 have green clays immediately below the level of the historic marsh. Further north on the cut-banks of Wadi al-'Unqiyya, we observed similar lacustrine clays to those in the bed of the Druz Marsh, but at an elevation that roughly corresponds with the identified elevation of paleolake shoreline benches (Fig. 7). This spatial relationship suggests that the green lacustrine clays were deposited when the water level rose in the Azraq Basin to form a lake that created a bay in what is now Wadi al- 'Unqiyya. The rough fit between the paleoshoreline data and the top of the green clay deposit is caused by a less than desirable error range (±3-5m) for the handheld GPS device we used for this data collection. The sediment exposures on the cut-banks of Wadi al- 'Unqiyya are shallow compared to those in the former marsh bed, ranging between 80 and 100 em. The green clays contain carbonate nodules near the surface that are greater than 1 em in size. Samples of these carbonates were taken for U-Series dating, giving us an age range of93,000 to 146,000 years BP. However, dating the carbonate itself means the age calculated represents the development of the carbonate nodules rather than the deposition of the green clays themselves (Kuzyakov et al. 2006). Therefore, the wet period responsible for

Basin Topography and Paleolake shorelines In order to position the above stratigraphic sequence into a regional context we draw your attention to five North Azraq topographic profiles (Fig. 1): 1) an upland shoreline deposit identified and dated by Abed et a!. (2008); 2) a transect across Wadi al-'Unqiyya; 3) a profile through the northern edge of the former marsh (Fig. 4); 4) a profile through the western edge of the former marsh; and 5) a profile through the southwest edge of the former marsh. The relations between the stratigraphy and the geomorphology of the basin can be understood through a series of profiles from the basalt to the bottom of the Druz Marsh basin (Fig. 6). Of particular importance is the relationship

depositing the green clays must be at the older limit of the date range or older than 146,000 years ago. Therefore, we hypothesize that the green clays are associated with the MIS 5e interglacial (ca.ll 0,000-130,000 years BP). Paleoenvironmental data from speleotherms in a cave northeast of the Azraq Basin suggests that the end of MIS 5a (ca. 80,000-70,000 years ago) was wetter than MIS 5e in northeast Jordan (Frumkin et al. 2008). Furthermore, in Qa' alMudawwara in the south of Jordan, Abed et al. (2000) identified two paleoshorelines dating to MIS 5e (116,000 ± 5,300 years BP) and MIS Sa (76,000 ± 8,200 years BP). In this case we cannot completely rule out a slightly younger timing for this considerable deposition of lacustrine clays in North Azraq without additional data. However, the upper limit of our date, 93,000 years BP, suggests the lacustrine clays were deposited prior to the end of MIS 5. Therefore, at present, the data corresponds most appropriately with a lacustrine deposition during MIS 5e. For the time being, accepting our current date and maintaining the interpretation of layers 2a and 2b as evidence of a transition from arid to moist conditions, we believe MIS 5e is responsible for the deposition of layers 3a and eroding the notches that form the paleoshore bench into the upland basalts. Additional evidence to support our hypothesized MIS 5e lake in North Azraq is the stratified

NORTH AZRAQ BASIN TOPOGRAPHIC PROFILES

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7. Paleoshoreline benches found in the upland basalts. Yellow circles are GPS points of prominent benches, similar to those shown in the images. Elevation summary statistics are presented for each cluster ofGPS points.

6. Correlation of North Azraq topographic profiles, see Figure I for locations of the profiles.

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Jordan s Prehistory: Past and Future Research

C.J.H Ames et a!.: Geoarchaeology and Prehistoric Transitions in the Azraq Druze

ed the Azraq-Umari Lake, although Abed et al. recognize the possibility that the two outcrops could represent separate but contemporaneous smaller lakes in both the Azraq and Umari areas. The fossil analysis of the bivalves indicates "that the salinity of the lake varied between brackish to fresh water throughout its history" (Abed et al. 2008:465), suggesting that even at a time when the water was at its highest known point during the past 350,000 years, the local environment was likely to be experiencing fluctuating evaporation and precipitation rates that were influencing the local flora and fauna, including hominins. This is perhaps a similar scenario as that hypothesized for the deposition of lacustrine clays of layers 3a, 3b and 3c that are interspersed with erosional unconformities and scattered lithic material.

Levallois lithic material we observed in a restoration pit behind Azraq Castle. Perhaps MP hominins were occupying the uplands during times of high water in North Azraq. Unfortunately we were unable to relocate the same sediment during our test excavation in 2009. However, if MP hominins were occupying what are now upland regions in Azraq it offers a potential ~xplanation for the paucity of known in-situ MP occupations. The areas are yet to be discovered and/or many of the areas have succumbed to erosion, the latter is supported by the presence of MP artifacts in the wadi bottoms (Copeland and Hours 1988; see Bisson this volume). Topographic profile 1 is immediately northeast of Wadi al-'Unqiyya on the upland flats where the basalts begin to plateau along the road to the Iraqi border. Here, and approximately 40km southeast of here at the Umari border point with Saudi Arabia, Abed eta!. (2008) identified two outcrops of a Cardium shell horizon. The Azraq locality could not be directly dated due to post-depositional alteration by pedogenic processes (see Abed et al. 2008:463 for details), but based on four single age determinations and one isochron measured from the Cardium shells from the Umari locality they estimate the age of the horizon to be between 316,000 and 346,000 years BP. This date associates the paleoshoreline deposit with the MIS 9 interglacial (ca. 310,000330,000 years BP). The lake has been designat-

Discussion Combining the stratigraphic and geomorphological data with our understanding of the historic marsh seasonal hydrological system (Fig. 2), we infer at least three paleoenvironmental conditions over the past 350,000 years in North Azraq (Fig. 8). Condition I occurs when the amount of rain is low, which reduces the exchange of water between the springs and the Qa' Azraq. However, relatively low temperatures in the winter prevent water from evaporating quickly and thus

Inferred paleoenvironmental conditions in the Druze Marsh

1 Low water wetland areas and small eutrophic lakes

2 High lake level, oligotrophic lake fed mainly by streams

3. Extremely dry conditions

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Dry or weok spring

DrawnedSpring

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8. Three hypothesized paleoenvironmental conditions over the past 350,000 years in North Azraq.

increase the flow of water into the aquifers and maintain the springs. Consequently, marshes and wetlands deeper than today, and/or eutrophic (oxygen-poor conditions) lakes, predominated in the Druz Marsh basin. Eutrophic conditions are produced by little exchange with the Qa' and a low, almost non-existent, influx of fluvial waters. Possible stages producing these conditions are the coldest parts of MIS 2, and probably the beginning and end of MIS 3. Evidence of this condition is present in Unit 3e and some eutrophic units from 'Ayn Qasiya that are dated to the Last Glacial Maximum (Rollefson eta!. 1997; Richter 2009; Richter et al. 2008). In our study, pollen associated with these deposits is predominantly from aquatic and desert plants. Condition 2 is produced when rains are abundant. The influx of water increases the flow of streams into the Qa' and creates large amounts of spring water. Water levels rise and drown the springs and marshes, resulting in the deposition of green clays. Hominin populations are occupying the higher elevation basalts to exploit resources associated with the lake. In some stages the lake would dry out and the population would return to the lake bed, following the water source and associated flora and fauna. Possible times of this high water level condition include MIS 5c and 5a. Intermittent lake drying may have occurred in MIS 5d, 5b, or the beginning of MIS 4. Such a condition, as in layer 3a, is associated with a fair amount of tree pollen and minimal pollen from aquatic plants. Part of MIS 5e may have had some moisture as well. As of yet, however, the stratigraphic resolution is too poor to determine whether the interglacial was wet or dry. U-series dates on carbonates from a paleosol below the Azraq castle provided a date of 130 ka, which is at the beginning of MIS-5e, whereas a carbonate nodule from Wadi Enoqiya produced an age estimate centered around 116 ka, which is towards the end ofMIS5e. Together these carbonate dates suggest a dry environment at both the beginning and end of the MIS 5e interglacial. Condition 3 occurs under extremely dry conditions. The springs dry out or become significantly slower. However, hominin populations and animals still congregate near the springs because they are the only source of water. Seasonal ponds occur that resemble the modem center of -77-

the Qa' in winter. Eolian processes predominate, which produce nebkhas and deflate the exposed lake bed. Occasionally beach deposits are present, but these are most likely to be the result of the receding lake from earlier wet periods. This condition is represented in layers 1c and 2a. The former is associated with Acheulean lithics and the latter seems to fill in an unconformity. No pollen has been preserved in these layers. Unfortunately, no dates exist for these layers. Carbonates from DM-2 provide aU-series age estimate centered around 151 ka, which suggests dryness during MIS 6. However, layer 2a in DM8, an eolian sand and silt, stratigraphically corresponds to either MIS-6 or MIS-5e. If the latter is correct, then there is a possibility that the MIS 5e interglacial was dry, as suggested by Frumkin et al. (2008, 2010). Accordingly, the MIS 5e interglacial was dry and the early glacial (MIS 5a-c) had wet spells. However, further research is needed to improve the resolution of local wet and dry periods for the last interglacial-glacial cycle in North Azraq. Prospective Work In tandem with geomorphologic and stratigraphic research, other paleoenv;ironmental studies are underway. Palynological and phytolith studies are providing support in relation to vegetation and climate change. A selective micromorphological analysis of the DM-8 stratigraphic succession is providing information about depositional environments and post-depositional pedogenic alterations. Additionally, bulk sediment analyses for organic matter content, magnetic susceptibility, and pH (see Pokines in this volume), will complement the study of soils and sediments. Future research in North Azraq aims to produce a 4-dimensional reconstruction of the former marsh bed, which is a volumetric model of the basin with a temporal component (Brown 2008). In order to accomplish this we have developed a 4-pronged research strategy that includes survey, trenching, excavation, and systematic coring. Many of these have already begun and were described above. Nevertheless, additional work is required to test and refine our hypothesized model of landscape evolution, water level fluctuation, and the impact on hominin populations in Azraq.

Jordan s Prehistory: Past and Future Research

C.JH. Ames et a!.: Geoarchaeology and Prehistoric Transitions in the Azraq Druze

Through additional survey we will map the modem topography and refine the elevation measurements for the upland benches eroded into the basalts with higher resolution differential GPS equipment. Continued trenching will build upon our current understanding of the stratigraphy while also providing sediment samples that will be examined for biological remains, used for geochemical analyses, as well as OSL, U-Series, and AMS dating. Such samples will also be available from additional controlled excavation. Finally, a systematic coring of the former marsh bed will be undertaken to provide stratigraphic and subsurface data while minimizing landscape alteration. After accounting for compression in the cores they will provide sediment depths and contribute to the volumetric model that is fundamental to the 4-dimensional reconstruction. Together this data is being compiled in a GIS database that can easily be made accessible to researchers and turned into an interactive educational tool.

Conclusion It has been acknowledged that the chronology of the Jordanian Paleolithic is still uncertain due to a predominance of non-contextualized finds and sites with only one temporal phase present (Copeland and Hours 1988). It is believed that the sequence will remain unclear "until we understand the sedimentological succession associated with the [stone] industries and its Palaeoclimatic meaning" (Copeland and Hours 1988:303). Recent work has begun to examine such paleoclimatic associations between sediments and archaeological collections in Azraq (Cordova 2007; Cordova et al. 2008; Cordova et al. 2009; Garrard et al. 1985, 1986, 1987, 1988, 1994; Richter 2009; Richter et al. 2008); most of which is focused on the last glacial maximum and the last glacial-interglacial transition (LGIT). The stratigraphic and geomorphologic data thus far obtained over the last two seasons show that the LGIT is one climatic fluctuation in a history of many for the Azraq region. At least five recorded sedimentary facies correspond to wet climatic conditions represented by lacustrine deposits (Units 1b, 3a, 3b, 3c, 3d) separated by erosional unconformities and pedogenic carbonates indicative of dry periods. A Cardium-rich -78-

shoreline deposit (Abed et al. 2008) and benches eroded into the upland basalts indicate that MIS 9 and MIS 5 (5c or Sa), respectively, sustained perennial lakes. Periods of transition between wet and dry are reflected in deposits of eutrophic lakes (Units 2b and 3e) and marshes (Units 4 and 5). Periods of extreme drought are reflected in eolian deposits (Ob, 1a, 1c, 2a, and the present silt dunes around the area) as well as stratigraphic unconformities and calcic horizons. Together this evidence implies that over the past 350,000 years, the North Azraq basin was subject to three distinct hydrological conditions related to seasonal temperatures and the amount and pattern of annual precipitation. An archaeological sequence from the Lower Paleolithic to the present is embedded in the cyclical succession of wet and dry periods described above. Therefore, our objective for the subsequent field seasons will be to refine the chronological sequence of wet and dry periods in the former Druz Marsh. This will allow paleoclimatic associations between sediments and archaeological collections that stretch back far beyond the LGIT. Additionally these associations will be reconstructed vertically and horizontally through the implementation of a 4-dimensional model of the changing landscape and associated paleoenvironments of North Azraq.

Acknowledgments We gratefully acknowledge the following people and institutions: For permission to conduct our research and for logistical support we would like to thank everyone at the Department of Antiquities in Amman and Azraq at the American Center of Oriental Research (ACOR). In particular we thank Dr. Fawwaz Al-Khraysheh, Mr. Ahmed Lash, Mr. Aktham Oweidi, Mr. Ahmed Sharma, Dr. Barbara Porter, Dr. Chris Tuttle and Ms. Kathy Nimri; For project funding we would like to thank the Social Science and Humanties Research Council of Canada (SSHRC); and for additional funding for students, personnel and equipment we thank SSHRC, JPAC-CIL, ACOR and ASOR. Christopher J. H. Ames Department of Anthropology, McGill University 855 Sherbrooke St. West Montreal, Quebec, Canada H3A 2T7

Carlos E. Cordova Department of Geography Oklahoma State University Stillwater, OK 74708 U.S.A. [email protected]

2007 Excavation Report and Discussion of Finds.

Annual of eth Department of Antiquities of Jordan 52:417-425.

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Jordan: The state ofResearch in 1·986:311-337. British Archaeological Reports - International Series 396. Oxford: BAR. Garrard, A.N, Betts, A., Byrd, B., Hunt, C. 1987 Prehistoric environment and settlement in the Azraq Basin: an interim report on the 1985 excavation season. Levant 19:5-25. Garrard, A.N, Byrd, B., Betts, A. 1986 Prehistoric environment and settlement in the Azraq Basin: an interim report on the 1984 excavation season. Levant 18:5- 24. Garrard, A.N, Byrd, B., Harvey, P., Hivernel, F. 1985 Prehistoric environment and settlement in the Azraq Basin. A report on the 1982 survey season. Levant 17:1-28. Ibrahim, K.M. 1996 The regional geology of Al-Azraq area. Map Sheet No. 35531 . Bulletin, Geological Mapping Division, Geology Directorate, Natural Resources Authority, Amman. Kuzyakov, Y., Shevtzova, E., Pustovoytov, K . 2006 Carbonate re-crystallization in soil revealed by 14 C labeling: experiment, model and significance for paleo-environmental reconstructions. Geoderma 131 :45-58.

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PRELIMINARY RESULTS FROM RECENT EXCAVATIONS AT THE EPIPALAEOLITHIC SITE OF Kharanah IV Lisa A. Maher, Tobias Richter, Jay T. Stock and Matthew Jones

Introduction Located in the eastern desert, the multi-component Epipalaeolithic site ofKharanah IV is notable for both its large size and high densities of lithic and faunal material. The site consists of a low mound, covering approximately 21,000 m2, and artefact-bearing horizons reach a depth of 1.5 m below the surface. In 2008 excavations at this site were renewed by the Epipalaeolithic Foragers in Azraq Project (EFAP), University of Cambridge, with the aim of better understanding the nature of occupation at the site and contextualising it within the Bpipalaeolithic of the larger Azraq Basin. The goals of this new work are 1) to continue excavations in two main areas (Areas A and B) excavated previously by Mujahed Muheisen and to correlate his findings with our new excavations, 2) to expand horizontally from these two areas to more fully expose particular archaeological features, including hearths, living floors, and possible hut architec-

ture, 3) to excavate deep soundings in several new areas in order to fully document the site's vertical stratigraphy in previously unexcavated parts of the site, 4) to conduct a geomorphological survey of the immediate area in order to contextualise the site within the larger environment and document landscape change since the Epipalaeolithic. Much of this work is ongoing. Here I present some preliminary results of our excavations, which include the discovery of a high-resolution sequence of early Epipalaeolithic hearths, pits, and living surfaces, and the possible remains of a structure in the middle Epipalaeolithic levels. I also discuss preliminary analyses of a unique microlith assemblage, human remains, worked bone and shell, and faunal and archaeobotanical material. The Site of Kharanah IV Kharanah IV is situated approximately 1 km southwest of Qasr Kharanah (Fig. 1). The site was originally noted by Harding (1959) and sur-

I. Topographic map ofKharanah IV. showing the locations of excavated areas, and the adjacent terraces and wadi.

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