INTRODUCTION
Humans are unprecedented agents of landscape change. Anthropogenic climate change continues to accelerate, and other activities such as urban expansion and animal grazing will likely cause drastic changes in ecosystems (Maestre et al., Reference Maestre, Eldridge, Soliveres, Kéfi, Delgado-Baquerizo, Bowker and García-Palacios2016; Dahinden et al., Reference Dahinden, Fischer and Knutti2017; IPCC, 2022). Dryland ecosystems comprise 41% of Earth's terrestrial surface, and 38% of the human population relies on them (Maestre et al., Reference Maestre, Eldridge, Soliveres, Kéfi, Delgado-Baquerizo, Bowker and García-Palacios2016). These ecosystems are especially sensitive to ecological change—small decreases in precipitation or increases in domesticate animal grazing can lead to a reduction in vegetation cover, with resultant impacts to water and food security (Asner et al., Reference Asner, Elmore, Olander, Martin and Harris2004; Maestre et al., Reference Maestre, Eldridge, Soliveres, Kéfi, Delgado-Baquerizo, Bowker and García-Palacios2016; Ball and Tzanopoulos, Reference Ball and Tzanopoulos2020). Climate models predict globally increasing temperatures that have the net effect of decreasing relative moisture in arid places (Stavi et al., Reference Stavi, Roque de Pinho, Paschalidou, Adamo, Galvin, de Sherbinin, Even, Heaviside and van der Geest2021). However, recent data are too brief to assess natural variability and long-term ecosystem dynamics (Dietl et al., Reference Dietl, Kidwell, Brenner, Burney, Flessa, Jackson and Koch2015). There is a need for longer-term records to investigate how changes in climate, particularly water availability, affect vegetation.
Southern Arabia is mainly hyperarid, but also hosts a biodiverse flora with a high level of endemism (Miller and Morris, Reference Miller and Morris1988; Ghazanfar, Reference Ghazanfar1998). The Dhofar Governorate of Oman is home to a unique cloud forest, with trees that intercept fog moisture from the seasonal Indian Ocean monsoon (khareef) (Hildebrandt et al., Reference Hildebrandt, Al Aufi, Amerjeed, Shammas and Eltahir2007). These conditions make the vegetation of Dhofar particularly sensitive to changes in temperature and precipitation: rainfall is correlated with vegetation cover, which is shown to be declining in the most arid locations in Dhofar (Ramadan et al., Reference Ramadan, Al-Awadhi and Charabi2021). Recent studies have additionally highlighted the threat of overgrazing of native vegetation by domesticated animals due to rapid economic growth over the last few decades, which has led to increased stocking rates of cattle and camels in Dhofar (Ghazanfar, Reference Ghazanfar1998; Galletti et al., Reference Galletti, Turner and Myint2016; Ball and Tzanopoulos, Reference Ball and Tzanopoulos2020). The preferential browsing of young shoots compared with adult trees prevents the regeneration of woody taxa, and there has been up to 10% loss of forest land cover in some areas of the cloud forest due to grazing alone (Galletti et al., Reference Galletti, Turner and Myint2016; Ball and Tzanopoulos, Reference Ball and Tzanopoulos2020). These changes have only been quantified over the last few decades as stocking rates reached current high levels (Galletti et al., Reference Galletti, Turner and Myint2016; Ball and Tzanopoulos, Reference Ball and Tzanopoulos2020). It is imperative to understand how both changes in climate and human activity dynamically influence vegetation, as human land use may amplify the effects of projected climate conditions.
One period that provides a case study for determining the vegetation response to increasing aridity is the end of the Holocene Humid Period. The termination of the Holocene Humid Period (~5.5 ka) led to decreased rainfall in southern Arabia and increasingly arid conditions (Morrill et al., Reference Morrill, Overpeck and Cole2003; Renssen et al., Reference Renssen, Brovkin, Fichefet and Goosse2003; Fleitmann et al., Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007, Reference Fleitmann, Burns, Pekala, Mangini, Al-Subbary, Al-Aowah, Kramers and Matter2011; Lézine et al., Reference Lézine, Bassinot and Peterschmitt2014; Ivory et al., Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021). Although this period has been well studied in places like North Africa, there are relatively few paleoclimate records from southern Arabia (Burns et al., Reference Burns, Matter, Frank and Mangini1998, Reference Burns, Fleitmann, Matter, Neff and Mangini2001; Fleitmann et al., Reference Fleitmann, Burns, Neff, Mudelsee, Mangini and Matter2004, Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007, Reference Fleitmann, Burns, Pekala, Mangini, Al-Subbary, Al-Aowah, Kramers and Matter2011; Kröpelin et al., Reference Kröpelin, Verschuren, Lézine, Eggermont, Cocquyt, Francus and Cazet2008). However, speleothem δ18O records preserve changes in precipitation during the last deglaciation from multiple locations in southern Arabia. These records suggest a gradual decline in precipitation beginning at ~8–7 ka (Fleitmann et al., Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007; Lézine et al., Reference Lézine, Bassinot and Peterschmitt2014). While it is likely that conditions were already semiarid in this region in the Early Holocene, these paleoclimate records indicate conditions became increasingly dry across the Holocene, such that perennial lakes disappeared and surface runoff became more limited (Hoorn and Cremaschi, Reference Hoorn and Cremaschi2004; Fleitmann et al., Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007; Lézine et al., Reference Lézine, Bassinot and Peterschmitt2014). The response of vegetation communities to these changes remains somewhat unclear.
To understand how ecosystems responded to decreasing rainfall over the Middle to Late Holocene, several previous paleoecological studies have been conducted in southern Oman and nearby Yemen. Estuarine cores from Oman provide near-continuous records of changes in coastal vegetation in the Middle to Late Holocene that show an increase in more saline- and drought-tolerant taxa (e.g., Amaranthaceae). This supports aridification by ~1.7–1.5 ka based on palynological and sedimentological evidence (Lézine et al., Reference Lézine, Saliège, Mathieu, Tagliatela, Mery, Charpentier and Cleuziou2002, Reference Lézine, Ivory, Braconnot and Marti2017; Hoorn and Cremaschi, Reference Hoorn and Cremaschi2004). There is also support for more wet phases that punctuated the trend in increasing aridity at ~2700–2300 and ~1700–1500 cal yr BP, when there was increased runoff to the estuaries (Hoorn and Cremaschi, Reference Hoorn and Cremaschi2004). However, information away from the coasts is patchy in both space and time. In Yemen, paleolakes provide insight into the wetter climate at the last deglaciation into the Early Holocene, as no perennial lakes exist in this region today (Lézine et al., Reference Lézine, Saliège, Robert, Wertz and Inizan1998, Reference Lézine2007). Pollen and sedimentological records from these lakes indicate that even during maximum humid conditions, there were seasonal periods of high evaporation that led to a persistence of a semiarid desert vegetation community in inland Yemen (Lézine et al., Reference Lézine2007). However, due to desiccation of most inland lakes by ~7 ka, evidence of vegetation change from sedimentary deposits in these areas after this time does not exist (Lézine et al., Reference Lézine2007). Pollen preserved in hyrax middens provides later records that suggest a semiarid woodland with tropical trees such as Terminalia at 5 ka at Wadi Sana, Yemen (Ivory et al., Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021). Little information exists about vegetation changes farther inland in Dhofar as aridification intensified from the mid-Holocene to the present.
Archaeological evidence suggests changes in settlement and mobility in Dhofar during the Holocene, lending some insight into changes in human land use over this time frame (Harrower et al., Reference Harrower, Senn and McCorriston2014 McCorriston et al., Reference McCorriston, Moritz, Buffington, Pustovoytov, Ivory, Abuazizeh, Purdue, Charbonnier and Khalidi2018; McCorriston and Harrower Reference McCorriston and Harrower2020). Nomadic pastoralism has been practiced in this region for at least 7000 yr and continues to be a culturally important lifeway (McCorriston et al., Reference McCorriston, Moritz, Buffington, Pustovoytov, Ivory, Abuazizeh, Purdue, Charbonnier and Khalidi2018). Archaeological evidence based on the construction of megalithic monuments in the desert and the lack of permanent habitation sites indicates pastoral groups were highly mobile and grazed their animals far inland (Harrower et al., Reference Harrower, Senn and McCorriston2014; McCorriston et al., Reference McCorriston, Harrower, Steimer, Williams and Senn2014, Reference McCorriston, Moritz, Buffington, Pustovoytov, Ivory, Abuazizeh, Purdue, Charbonnier and Khalidi2018). This was during an interval when paleoclimatic records suggest wetter than modern conditions (~7–5 ka) (Fleitmann et al., Reference Fleitmann, Burns, Neff, Mudelsee, Mangini and Matter2004, Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007). During a period of increased aridity in the Late Holocene (~2–1 ka), pastoralists built more permanent settlements closer to the coast (McCorriston et al., Reference McCorriston, Harrower, Steimer, Williams and Senn2014; McCorriston and Harrower Reference McCorriston and Harrower2020). The ecological effects of ancient pastoralism and changes in settlement patterns are not well understood. Modern pastoral activity can have surprising impacts on vegetation in these arid regions that are not always degradational. For example, grazing and browsing can maintain grasslands and domesticate dung increases nutrient input to dry soils (Brierley et al., Reference Brierley, Manning and Maslin2018). Assessing changes in vegetation in this region is important for understanding the persistence, and hopefully the continued sustainability, of pastoralism under changing climate conditions. Moreover, teasing apart climate- and human-driven mechanisms of vegetation change is important for making more accurate predictions about changes to semiarid pastoral landscapes and designing sustainability initiatives to mitigate them.
In this study, we present pollen and bulk stable isotope data from rock hyrax (Procavia capensis) middens collected in the Dhofar Governorate of Oman. We use thin (<5 cm) middens that represent individual, temporally averaged samples, with the oldest radiocarbon age at ~4000 cal yr BP. Rock hyrax middens serve as well-established paleoecological archives in arid ecosystems, preserving pollen, macrofossils, and isotopic information for thousands of years (Scott and Cooremans, Reference Scott and Cooremans1992; Scott and Woodborne, Reference Scott and Woodborne2007; Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012; Ivory et al., Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021). The records presented here provide paleoecological information after the onset of decreasing precipitation in this region at the end of the Holocene Humid Period to the present. While future conditions in Dhofar are likely to be drier than those seen in the last 4000 yr, this record provides a long-term view of vegetation response to climate change in this unique, biodiverse dryland ecosystem (Dahinden et al., Reference Dahinden, Fischer and Knutti2017). This can help inform predictions for southern Arabia as well as semiarid drylands that are expected to experience aridification similar to that seen across the Holocene in Dhofar.
Modern setting
The physiography of southern Oman is strongly characterized by the steep south-facing escarpments of the Dhofar Mountains. These mountains are mainly composed of Tertiary limestone, with a karst net that forms caves and rock shelters (Miller and Morris, Reference Miller and Morris1988; Cremaschi et al., Reference Cremaschi, Zerboni, Charpentier, Crassard, Isola, Regattieri and Zanchetta2015). A fault system crosscuts the north-dipping limestone strata, which is mainly oriented east-west (Zerboni et al., Reference Zerboni, Perego, Mariani, Brandolini, Al Kindi, Regattieri, Zanchetta, Borgi, Charpentier and Cremaschi2020). At the highest elevations, approximately 850 m above sea level, the landscape becomes a plateau inset by northward-draining wadi systems (Miller and Morris, Reference Miller and Morris1988; Zerboni et al., Reference Zerboni, Perego, Mariani, Brandolini, Al Kindi, Regattieri, Zanchetta, Borgi, Charpentier and Cremaschi2020). The Tertiary carbonates are incised by these dry riverbeds, which are covered with large gravel alluvium (Al-Mashaikhi et al., Reference Al-Mashaikhi, Oswald, Attinger, Büchel, Knöller and Strauch2012). A lack of soil in the desert inland from the coast creates a landscape of large, bare carbonate outcrops that form the wadi walls (Zerboni et al., Reference Zerboni, Perego, Mariani, Brandolini, Al Kindi, Regattieri, Zanchetta, Borgi, Charpentier and Cremaschi2020).
The Dhofar Governorate is predominantly arid. The coastal region receives approximately 120–150 mm of precipitation per year and has a mean annual temperature of 25.7°C based on data from the Salalah airport weather station (1970–1990) (Fleitmann et al., Reference Fleitmann, Burns, Neff, Mudelsee, Mangini and Matter2004, Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007; Cremaschi et al., Reference Cremaschi, Zerboni, Charpentier, Crassard, Isola, Regattieri and Zanchetta2015). However, hyperarid conditions prevail farther inland in the Nejd Desert, which receives an average of 30 mm of precipitation per year based on observations from the Thumrait weather station (1980–2015) (Almazroui et al., Reference Almazroui, Islam, Jones, Athar and Rahman2012). These two weather stations are denoted on the map in Figure 1. Most of the precipitation in this region occurs during the northern summer (June–September) (Fleitmann et al., Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007), when the Indian monsoon brings dense fog to the coastal regions of Dhofar, increasing relative humidity to as much as 97% (Patzelt, Reference Patzelt2015). This fog forms as moisture-laden air passes over the cool surface waters off the coast (Miller and Morris, Reference Miller and Morris1988). As the fog moves inland, it becomes trapped against the slopes due to a temperature inversion, blanketing the escarpment with thick cloud cover that generally does not extend past the crest of the escarpment (Miller and Morris, Reference Miller and Morris1988).
Map of Dhofar depicting the four ecological zones. The midden sampling locations are shown by the boxes. Inset shows the geopolitical boundaries of Oman on the Arabian Peninsula.
The modern vegetation can be categorized into four ecological zones from south to north (coastal plain, escarpment, plateau, and Nejd Desert), which encompass changes in elevation and climate conditions, as well as the dominant taxa (Miller and Morris, Reference Miller and Morris1988). The coastal plain is a flat, low-elevation band that stretches from the coast to the foothills of the escarpment. The vegetation in this zone is extremely sparse due to overgrazing and other human activities, but plants such as Aerva javanica and Heliotropium spp. can be found on rockier soils (Miller and Morris, Reference Miller and Morris1988). The escarpment is home to the seasonal cloud forests composed of deciduous trees, notably Terminalia dhofarica and Maytenus dhofarensis, with an understory of grasses (Poaceae) and other herbs (Merremia spp., Heliotropium spp.) (Patzelt, Reference Patzelt2015). These trees, particularly T. dhofarica, are reliant on moisture from the monsoon fog. Terminalia dhofarica intercepts moisture directly from the air during the khareef to increase net water availability locally (Hildebrandt et al., Reference Hildebrandt, Al Aufi, Amerjeed, Shammas and Eltahir2007; Friesen et al., Reference Friesen, Zink, Bawain and Müller2018). The plateau is a grassland with isolated trees such as Ficus vasta (Miller and Morris, Reference Miller and Morris1988; Buffington and McCorriston, Reference Buffington and McCorriston2019). On the distal reaches of the plateau beyond the monsoonal fog, Boswellia sacra (frankincense) is commonly found (Patzelt, Reference Patzelt2015). The farthest inland is the Nejd Desert, which is the driest sector in the region (Almazroui et al., Reference Almazroui, Islam, Jones, Athar and Rahman2012). This zone is characterized by isolated trees (Senegalia spp., Boscia, Maerua, Ficus salicifolia) and sparse herbaceous cover (Heliotropium spp., Cornulaca) (Miller and Morris, Reference Miller and Morris1988; Ghazanfar, Reference Ghazanfar2004; Patzelt, Reference Patzelt2015). Table 1 highlights the dominant taxa in each of these areas.
The four ecological zones of Dhofar and their dominant vegetation taxa.
Hyrax middens as paleoenvironmental archives
Various types of animal middens have been successfully employed for paleoenvironmental analyses. These archives represent different spatial and temporal scales, dictated by the behavior of the animal and the manner in which they are deposited (Cole, Reference Cole1990; Anderson and Van Devender, Reference Anderson and Van Devender1995; Scott et al., Reference Scott, Marais and Brook2004; Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012). In the dry regions of western North America, packrat (Neotoma) midden studies have revealed changes in local flora within ~10–100 m of den sites through pollen and macrofossil studies and, more recently, ancient DNA (Cole, Reference Cole1990; Anderson and Van Devender, Reference Anderson and Van Devender1995; Fisher et al., Reference Fisher, Cole and Anderson2009; Moore et al., Reference Moore, Tessler, Cunningham, Betancourt and Harbert2020). Packrats collect plant matter and other materials, creating “garbage piles” protecting the entrances of their dens (Cole, Reference Cole1990). Through the defecation and urination of the packrats, this garbage pile will become an indurated mass, or midden (Cole, Reference Cole1990; Anderson and Van Devender, Reference Anderson and Van Devender1995; Fisher et al., Reference Fisher, Cole and Anderson2009). Analyses of modern packrat middens and local vegetation show high agreement, indicating that fossil middens are a reliable archive of past environments (Cole, Reference Cole1990; Anderson and Van Devender, Reference Anderson and Van Devender1995; Fisher et al., Reference Fisher, Cole and Anderson2009). These samples are processed through dissolution in water, then a sieving process that separates macrofossil and microfossil fractions (Van Devender et al., Reference Van Devender, Burgess, Piper and Turner1994; Moore et al., Reference Moore, Tessler, Cunningham, Betancourt and Harbert2020). Each midden is dated and treated as one sample at an individual point in time (Van Devender et al., Reference Van Devender, Burgess, Piper and Turner1994; Anderson and Van Devender, Reference Anderson and Van Devender1995).
Rock hyrax middens have emerged as a powerful tool for similar paleoecological studies in the arid regions of Africa and Arabia (Scott and Woodborne, Reference Scott and Woodborne2007; Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012; Ivory et al., Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021). Rock hyraxes are small mammals that resemble rodents but are in fact most closely related to elephants. They can eat a wide variety of plants and tolerate a large range of temperature and precipitation conditions (Sale, Reference Sale1965; Rübsamen et al., Reference Rübsamen, Hume and von Engelhardt1982; Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012; Mohamed, Reference Mohamed2019). Generally, middens are deposited in caves and rocky overhangs as compacted deposits of crystallized urine (hyraceum) and fecal pellets (Gil-Romera et al., Reference Gil-Romera, Lamb, Turton, Sevilla-Callejo and Umer2010; Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012). Pollen and other paleoenvironmental indicators are brought into the caves on the feet or fur of hyraxes and blown in via eolian deposition, then trapped in the sticky hyraceum (Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012). Plant matter consumed by the hyraxes also passes through their digestive systems and is preserved in their dung (Scott et al., Reference Scott, Marais and Brook2004; Scott and Woodborne, Reference Scott and Woodborne2007; Gil-Romera et al., Reference Gil-Romera, Lamb, Turton, Sevilla-Callejo and Umer2010; Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012). Stable carbon isotope analyses of fecal pellets and hyraceum reflect the input of C3 and C4 vegetation, and nitrogen isotope studies can reveal changes in relative moisture (Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012; Ivory et al., Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021). Middens can differ in thickness and the amount of hyraceum versus fecal pellets, and thus can have varying degrees of dietary bias and represent disparate temporal scales (Scott and Cooremans, Reference Scott and Cooremans1992; Scott et al., Reference Scott, Marais and Brook2004; Gil-Romera et al., Reference Gil-Romera, Scott, Marais and Brook2006; Scott and Woodborne, Reference Scott and Woodborne2007; Chase et al., Reference Chase, Meadows, Scott, Thomas, Marais, Sealy and Reimer2009, Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012).
In southern Africa, massive middens composed primarily of hyraceum have been discovered, providing paleoenvironmental insight for the late Pleistocene and Holocene (Chase et al., Reference Chase, Meadows, Scott, Thomas, Marais, Sealy and Reimer2009, Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012; Carr et al., Reference Carr, Boom and Chase2010). These types of middens can be subsampled for isotope and pollen analyses, much like a sediment core, and the data can be interpreted as a time series (Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012). However, thinner middens consisting of indurated dung material have also proved a useful archive of the same paleoecological indicators (Scott and Cooremans, Reference Scott and Cooremans1992; Scott et al., Reference Scott, Marais and Brook2004; Gil-Romera et al., Reference Gil-Romera, Scott, Marais and Brook2006; Scott and Woodborne, Reference Scott and Woodborne2007; Ivory et al., Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021). While these contain a higher dietary input from fecal material, analyses of modern dung middens from South Africa illustrate that their pollen spectra are negligibly different from pollen spectra of surface soils (Scott and Cooremans, Reference Scott and Cooremans1992). Moreover, studies of hyrax diet and behavior from both Africa and Arabia demonstrate that hyraxes are generalists and have few dietary restrictions (Sale, Reference Sale1965; Mohamed, Reference Mohamed2019).
The methodology for processing these samples is also different. Hyraceum middens are typically radiometrically dated, drilled for isotopic analyses, then processed for pollen and other indicators through the midden's growth axis (Carr et al., Reference Carr, Boom and Chase2010; Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012). Processing of thin dung middens follows a protocol similar to the one described for packrat middens: they are first disaggregated in water, then sieved to obtain macrofossil and microfossil fractions (Van Devender et al., Reference Van Devender, Burgess, Piper and Turner1994; Scott and Woodborne, Reference Scott and Woodborne2007; Ivory et al., Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021). Because of the differences in material and sampling, thin middens are interpreted as single, variably time-averaged samples. Hyraceum middens can provide long term (103–104 yr) paleoecological sequences with single data points averaged over ~101–102 yr, whereas paleoecological data from dung middens are averaged over the period of midden deposition and include more dietary information (Scott and Cooremans, Reference Scott and Cooremans1992; Gil-Romera et al., Reference Gil-Romera, Scott, Marais and Brook2006; Scott and Woodborne, Reference Scott and Woodborne2007; Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012; Ivory et al., Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021).
In this study, we obtained thin (<5 cm) rock hyrax middens consisting of indurated dung pellets cemented with crystallized urine. To process these middens and conduct pollen analysis, we utilized the same approach that has been successful for both packrat middens and other fossil hyrax dung middens in South Africa (Van Devender et al., Reference Van Devender, Burgess, Piper and Turner1994; Scott and Woodborne, Reference Scott and Woodborne2007; Ivory et al., Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021). The presence of fecal matter introduces a degree of dietary bias in these samples. However, we conducted a comparison of pollen abundances from modern middens with botanical information from Dhofar and determined that the signal recorded within the middens is a good representation of local vegetation. To assess the period over which thin middens accumulate, Ivory et al. (Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021) obtained multiple radiocarbon dates from the same midden, which resulted in ages that were not significantly different. This analysis was conducted on multiple middens. Based on this analysis from nearby Yemen on similar middens, we assume the middens from our study represent decades to ~100 yr of deposition. As such, we interpret each midden as one sample, and the data as an average of local vegetation over ~100 yr.
METHODS
Pollen analysis was conducted on 13 modern hyrax middens across a large geographic area and spans the four ecological zones (Table 2, Supplementary Material 1). These were determined to be modern through radiocarbon dating or if the samples were not compacted and included fresh dung, as was the case for all middens collected closer to the coast. In these regions, prevailing moist conditions during the monsoon season lead to the disintegration of middens; older middens are not typically preserved. Four samples were taken from the distal plateau (Wadi Ayun), two from a drainage system in the western Nejd (Wadi Ghadun), and three from the east Nejd (Wadi Dhahabun). Two samples were collected from the coastal plain close to the base of the escarpment. Two samples of fresh camel (Camelus dromedarius) dung were also collected on the escarpment, where no hyrax middens were found. These samples were then compared with published botanical literature from the Dhofar region as well as vegetation surveys (provided in Supplementary Material 2) to assess the representativity of flora within this archive (Miller and Morris, Reference Miller and Morris1988; Ghazanfar, Reference Ghazanfar1998, Reference Ghazanfar1999, Reference Ghazanfar2004; Raffaelli et al., Reference Raffaelli, Mosti and Tardelli2003; Hildebrandt et al., Reference Hildebrandt, Al Aufi, Amerjeed, Shammas and Eltahir2007; Patzelt, Reference Patzelt2015). The modern samples were also compared with four submodern middens from the east Nejd (110–160 cal yr BP) to assess historic changes in vegetation.
Modern midden sampling locations, accelerator mass spectrometry (AMS) radiocarbon dates, calibrated ages, and bulk stable isotope information.
Additionally, pollen analysis was completed on fossil middens in the Nejd Desert to establish a record of vegetation change over the last 4000 yr. To create the fossil pollen record, 26 rock hyrax middens were collected over three field seasons from February 2017 through October 2018 (Table 3). Twenty-two fossil middens and one modern midden were collected from the east Nejd, while three additional modern midden samples from the distal plateau farther to the west were used to compare a wide geographic range of modern vegetation with the recorded fossil vegetation (Fig. 1). Surveying for middens consists of examining small natural caves in cliffs and looking for fecal pellets in and around these sheltered locations. The presence of these pellets helped identify caves that could contain middens. Once discovered, these middens were carefully extracted from the caves using a chisel and hammer, keeping them as intact as possible. The samples were then wrapped in plastic to avoid contamination before shipment. A photograph of a representative midden as well as a midden in situ are shown in Figure 2.
Fossil midden sampling locations, accelerator mass spectrometry (AMS) radiocarbon dates, calibrated ages, and bulk stable isotope information.
a UGAMS, University of Georgia Center for Applied Isotope Studies for Accelerator Mass Spectrometry.
Pictures of representative rock hyrax middens.
Palynological analysis
This study involves a sampling protocol for thin (<5 cm) middens. A minimum of 100 g of material, representing the entire vertical thickness of the midden, was disaggregated in 1 L of deionized water. This solution was sieved at 500 μm to remove fecal pellets and separate macrobotanicals. The <500 μm fraction was then used for pollen and microcharcoal analyses. A standard volume (45 mL) from each disaggregated sample was processed using the extraction method of Faegri and Iversen (Reference Faegri and Iversen1989). Hydrochloric acid was used to remove carbonates, and hydrofluoric acid was used to remove silicates. Acetolysis removed most organic material from the samples. The samples were sieved at 180 and 10 μm to remove large particulates and clays, respectively. Lycopodium spores were added to each sample to calculate pollen concentrations. The pollen residue was suspended in glycerin and mounted on glass slides for microscopy, and an average of 354 pollen grains (including fern spores) per sample were counted. For four samples, pollen counts fell below 300 but were still >250 grains. For two samples, WP107-2B and WP149-2, 44 and 186 grains were counted, respectively, due to issues of preservation. Microcharcoal pieces that were >10 μm were also counted.
Pollen identifications were made using the African Pollen Database (APD; Lézine et al., Reference Lézine, Ivory, Gosling, Scott, Runge, Gosling, Lézine and Scott2021), the pollen atlas of Bonefille and Riollet (Reference Bonefille and Riollet1980), and a collection of reference slides from the Penn State Paleoecology Lab. Pollen taxa were categorized by plant habit, with the most predominant types being arboreal, herbs, and indeterminate, with indeterminate indicating there are multiple plant habits represented by that taxon. Taxonomic nomenclature and plant habit follow the APD (Vincens et al., Reference Vincens, Lézine, Buchet, Lewden and Le Thomas2007; Lézine et al., Reference Lézine, Ivory, Gosling, Scott, Runge, Gosling, Lézine and Scott2021). Pollen morphotypes for the genus Senegalia were differentiated based on their exine texture. Smooth exines were classified as Senegalia I, gemmate as Senegalia II, and reticulate as Senegalia III (Guinet and Vassal, Reference Guinet and Vassal1978).
Certain groups of taxa were defined based on their affiliations to wetter or drier areas in Dhofar, as well as whether they are considered grazing indicators. Grazing indicators in this setting are plant taxa that are avoided by domesticate animals, and therefore tend to be in higher abundances relative to other plants in highly grazed areas. Of these taxa, Dodonaea viscosa, Cassia-type, Heliotropium, and Cornulaca/Aerva-type are observed in the pollen record (Dereje and Udén, Reference Dereje and Udén2005; Brinkmann et al., Reference Brinkmann, Patzelt, Dickhoefer, Schlecht and Buerkert2009). Mesic-affiliated taxa are arboreal pollen taxa that are generally found in moister areas of Dhofar, such as the escarpment and plateau; these are identified as T. dhofarica, Boscia/Cadaba, Maytenus, Ficus, and B. sacra (Miller and Morris, Reference Miller and Morris1988; Patzelt, Reference Patzelt2015). Nejd associations are defined here as the most common pollen taxa found today in the dry Nejd: Amaranthaceae, Senegalia I, Commiphora, Salvadora persica, and Senegalia III (Miller and Morris, Reference Miller and Morris1988; Patzelt, Reference Patzelt2015).
Raw pollen counts were converted to relative abundances using a total of pollen grains and fern spores (APD). Concentrations were calculated by first determining the particles per milliliter of disaggregated sample, then using the sample mass that was rehydrated to calculate particles per gram of sample. A pollen diagram based on the relative abundances (%) was generated in Tilia (Grimm, Reference Grimm1987), and pollen zones were quantitatively determined using the CONISS program (Grimm, Reference Grimm1987). CONISS cluster analysis is stratigraphically constrained and uses the sum of squares (Grimm, Reference Grimm1987). Detrended correspondence analysis (DCA) was conducted using the vegan package in R (ter Braak Reference ter Braak1985; Oksanen et al., Reference Oksanen, Blanchet, Kindt, Legendre, Minchin, O'Hara, Simpson, Solymos, Stevens and Wagner2013; RStudio Team, 2020). Taxa with maximum abundances less than 2% within a single sample and taxa with only one occurrence were excluded from the DCA and the CONISS. The relative abundances were Wisconsin-transformed and detrended using 26 segments. The axes were rescaled using four iterations. Sample and taxa scores were plotted on the first two axes, and the samples were assigned colors according to their CONISS cluster membership.
Radiocarbon dating and stable isotopes
After the middens had been disaggregated, the sieved >500-micron fraction was separated and dried. This fraction included plant macrobotanicals and fecal pellets. Ten fecal pellets were randomly selected from the sieved material and homogenized, then sent to the University of Georgia Center for Applied Isotope Studies for Accelerator Mass Spectrometry (AMS) radiocarbon dating. More than one pellet was used to obtain an average age for the sample. There is the possibility that these pellets were deposited and not cemented by hyraceum for a period of time, and thus have ages not directly representative of fossil pollen in the hyraceum fraction. However, given the nature of the middens as thin, dung-rich accumulations, it is likely they formed within a relatively brief amount of time (101–102 yr). Because of this, we interpret the data as averaged across this time frame (Scott and Woodborne, Reference Scott and Woodborne2007; Ivory et al., Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021). For two samples (WP38-3a 4-6 and WP50-2 0.5-2), radiocarbon dates were obtained on hyraceum drilled out of the solid sample before disaggregation. Calibrated ages were determined using Calib 8.20 (Stuiver and Reimer, Reference Stuiver and Reimer1993) and the Intcal20 calibration curve (Reimer et al., Reference Reimer, Austin, Bard, Bayliss, Blackwell, Bronk Ramsey and Butzin2020).
Bulk δ13C and δ15N were also measured on the same homogenized samples at the same laboratory using gas chromatography isotope ratio mass spectrometry (Table 3). Bulk δ13C values measured on fecal pellets should be largely reflective of the carbon isotopes of undigested plant material and can be used to infer changes in C3 and C4 vegetation (Ehleringer et al., Reference Ehleringer, Cerling and Helliker1997; Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012). Analyses of rock hyrax middens in southern Africa and Yemen have demonstrated a link between bulk δ15N and relative moisture, wherein the nitrogen isotope composition in the feces reflects that of the consumed plant tissue, which is absorbed from the pool of nitrogen in the soil (Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012; Craine et al., Reference Craine, Brookshire, Cramer, Hasselquist, Koba, Marin-Spiotta and Wang2015: Ivory et al., Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021). This relationship has also been observed in feces from other herbivores (Díaz et al., Reference Díaz, Frugone, Gutiérrez and Latorre2016). Generally, δ15N is negatively correlated with mean annual precipitation (MAP) on a global scale, and thus has an inverse relationship with soil moisture (Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012; Wang et al., Reference Wang, Wang, Liu, Wu, Lü, Fang and Cheng2014). However, nitrogen cycling in soils is a complicated process that may be driven by other mechanisms in arid regions (Wang et al., Reference Wang, Wang, Liu, Wu, Lü, Fang and Cheng2014; Craine et al., Reference Craine, Brookshire, Cramer, Hasselquist, Koba, Marin-Spiotta and Wang2015; Díaz et al., Reference Díaz, Frugone, Gutiérrez and Latorre2016).
To evaluate the relationship between δ15N and moisture in the middens, we compared the bulk δ15N with speleothem records of δ18O from the Qunf and Defore Caves (Fleitmann et al., Reference Fleitmann, Burns, Neff, Mudelsee, Mangini and Matter2004, Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007). While these indicators reflect different aspects of hydroclimate, speleothem δ18O can be used as a proxy for precipitation, specifically monsoon rainfall, which represents most of the MAP in this region (Fleitmann et al., Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007). Values of δ15N traditionally have an inverse relationship with MAP, but this correlation may change in very arid places (Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012; Wang et al., Reference Wang, Wang, Liu, Wu, Lü, Fang and Cheng2014; Díaz et al., Reference Díaz, Frugone, Gutiérrez and Latorre2016). The Qunf Cave (17°10′N, 54°18′E) δ18O data were sourced from the National Oceanographic and Atmospheric Administration paleoclimatology database. To obtain submodern (~200–50 BP) δ18O values, which are missing due to a hiatus at Qunf Cave, data were extracted from a speleothem from nearby Defore Cave (17°07′N, 54°05′E) that covers this interval (Fleitmann et al., Reference Fleitmann, Burns, Neff, Mudelsee, Mangini and Matter2004).
The temporal resolution of the Qunf Cave speleothem record was much higher than that of the middens, which were temporally averaged (Fleitmann et al., Reference Fleitmann, Burns, Neff, Mudelsee, Mangini and Matter2004, Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007; Ivory et al., Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021). To help account for this, the 1σ range (68.3% probability) of the calibrated ages for the midden samples was used determine an age range over which to average the δ18O data from the speleothem record. A set of three samples (WP38-3a 4-6, 665 cal yr BP; WP50-2 0.5-2, 853 cal yr BP; WP38-2B, 1461 cal yr BP) with particularly high measured values of δ15N (6.7–12.6‰ above the average of 9.5‰) were not included in this analysis. Two of these (WP38-3a 4-6 and WP50-2 0.5-2) were measured on hyraceum rather than fecal pellets. Rock hyraxes concentrate their urine to preserve water as an adaptation to their arid environment, which likely affects the δ15N value (Rübsamen et al., Reference Rübsamen, Hume and von Engelhardt1982; Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012). The third sample (WP38-3a 4-6, 21.3‰) was removed, as it fell far beyond the calculated standard deviation (7.90 ± 3.43‰). Modern samples and five samples with median ages 1922–1566 cal yr BP were also excluded due to a lack of coverage in the speleothem δ18O data. The averaged speleothem δ18O values were then plotted against the bulk δ15N from each midden. For samples with overlapping 1σ ranges, each δ15N value was plotted individually. Error bars representing the 95% confidence interval were added for the δ18O averages, then a linear regression was conducted.
RESULTS
Modern pollen
On the coastal plain near the base of the escarpment, the samples are dominated by Dracaena (31.0%), Poaceae (17.6%), and Senegalia III (6.8%). The pollen taxa in highest abundance from the camel dung collected in the escarpment mountains were Poaceae (67.6%), T. dhofarica (7.4%), and Suaeda (6.3%). In the distal plateau samples, the most abundant taxa are S. persica (17.7%), Poaceae (9.2%), D. viscosa (8.3%), Cocculus pendulus (7.9%), and Senegalia III (7.3%). Here, the abundance of B. sacra is highest (6.5%). In the western Nejd, S. persica (19.0%), Ficus (14.0%), Poaceae (10.3%), Senegalia III (9.5%), and Ziziphus-type (8.9%) are all relatively abundant. Cyperaceae pollen also occurs in a relatively higher proportion (7.8%). Modern east Nejd samples are characterized by Polycarpon-type (Reseda) (39.2%), Kohautia (12.9%), Poaceae (8.7%), and Senegalia III (7.2%). The submodern samples from east Nejd have a lower pollen abundance of Polycarpon-type (Reseda) (12.0%) and Kohautia (1.7%). Senegalia III (9.7%) is higher in abundance. The samples contain higher percentages of Ficus (8.2%) and Poaceae (15.2%) (Fig. 3).
Pollen diagram of modern hyrax middens and two camel dung samples, in order from north to south. The middens are grouped by their ecological zone (east Nejd, west Nejd, distal plateau, escarpment, coastal plain). The two escarpment samples are camel dung specimens. Submodern hyrax middens are included with their median calibrated ages. Pollen abundances are on the x-axis. The green shade indicates tree pollen habits, gray, indeterminate habits, and yellow, herbaceous pollen habits. The CONISS dendrogram is plotted on the right.
CONISS cluster analysis reveals two compositionally distinct groups of samples; those collected from the escarpment and coastal plain ecological zones cluster as one group, and samples from the Nejd and distal plateau locations cluster as the other (Fig. 3). In the DCA, Nejd samples cluster with common modern taxa observed within 100 m of the midden caves such as Senegalia (4.3%) and S. persica (12.6%) (Fig. 4). Two samples of fresh camel dung collected from the escarpment region have pollen representative of modern cloud forest taxa, notably T. dhofarica (7.4%). Grazing indicator pollen taxa are in highest abundance today in samples from the distal plateau (13.2%). Submodern (160–110 cal yr BP) samples in the east Nejd reveal higher abundances (10.7%) of grazing indicators compared with modern abundances in this region (7.9%).
Detrended correspondence analysis (DCA) of all modern samples (right), and including submodern samples (left). Samples are color coded by ecological zone.
Fossil pollen zones
Pollen analysis of the fossil middens revealed a diverse flora, with 134 total pollen taxa identified. Preservation was variable among the samples, with a range of percent broken grains of 0–11.9%. Most samples (23) had good preservation (broken grains <10%), while three had higher abundances of broken pollen grains (WP45-2, WP153-2, and WP38-3a 4-6). The average pollen concentration of the samples was 12,825.13 particles/g. Zonation of the pollen stratigraphy was determined using the CONISS dendrogram, which splits the assemblages into two distinct sets of samples, the fossil samples and the modern. The fossil samples are then subdivided into groups A and B, then again into A1, A2, B1, and B2. These subzones were based on the two next-highest branch heights in the dendrogram. The percentages given are zonal average abundances, except for those that refer to a single sample and are specified as such. Pollen taxa were grouped within the pollen diagram by plant habit (APD; Vincens et al., Reference Vincens, Lézine, Buchet, Lewden and Le Thomas2007; Lézine et al., Reference Lézine, Ivory, Gosling, Scott, Runge, Gosling, Lézine and Scott2021). The trends described in this section refer to the pollen diagram in Figure 5.
Pollen diagram of selected taxa from east Nejd fossil middens. Abundances are plotted on the x-axis and age in calibrated years BP on the y-axis. The four modern samples are plotted individually. The green shade indicates tree pollen habits, gray, indeterminate habits, and yellow, taxa with herbaceous pollen habits. Pollen zones determined via CONISS cluster analysis are represented by the column on the right.
Zone A1 (4038–3233 cal yr BP)
This pollen zone includes the two oldest samples. Herbaceous pollen comprised 4.0–17.0% of total pollen in each sample, while arboreal pollen was 27.0–57.0% of the total pollen. The most abundant herbaceous taxa were Poaceae (3.0%) and Kohautia (1.7%), but these were fairly low in abundance compared with the rest of the pollen record. Boswellia sacra (10.8%), Ficus (17.9%), and Boscia/Cadaba (5.2%) pollen were the most dominant tree taxa. The liana Cocculus pendulus was also a dominant pollen taxon (10.8%) in this zone.
Zone A2 (3103–1466 cal yr BP)
There are eight samples within this zone, which bracket an 1100-yr gap from 2920 to 1651 cal yr BP. The oldest sample (3103 cal yr BP) contained notably high abundances of Combretaceae pollen (31.2%), which mainly consisted of T. dhofarica (30.9%). The third sample occurred after the gap in the record, and at this time there was a transition to increased abundances of herbaceous pollen taxa (21.2%) on average in the rest of the samples. There was a pronounced increase in Kohautia pollen (10.3%), as well as an increase in pollen from Poaceae (8.2%) in the younger six samples. Tree pollen (30.7%) decreased from the previous zone but remained abundant. Ficus (7.7%) decreased in this zone.
Zone B1 (1461–115 cal yr BP)
This zone contains nine samples. Herbaceous pollen taxa (21.8%) remained similarly abundant from the prior zone, while tree pollen (18.7%) decreased further in abundance. The transition to this zone was dominated by pronounced increases in Commiphora (11.3%) and Cyperaceae (22.3%) pollen in the oldest sample. Pollen from the Amaranthaceae family (12.0%) also increased during this interval.
Zone B2 (114–107 cal yr BP)
This pollen zone consists of three submodern samples. Herbaceous pollen taxa (22.9%) were still abundant, but there was also a significant increase in tree pollen (29.1%). Ficus pollen (12.0%) was the most abundant tree taxon. Poaceae pollen (10.6%) became more abundant than in previous intervals, while Amaranthaceae pollen (5.3%) decreased.
Modern
This zone consists of all the modern samples from both the east Nejd and the distal plateau. These samples were characterized by high abundances of tree pollen (37.9%). Herbaceous pollen (22.5%) remained at an abundance consistent with the previous zone. There was a marked increase in pollen from the trees such as S. persica (15.1%) and D. viscosa (6.7%), as well as an increase in Senegalia III (4.4%). Poaceae pollen (12.2%) increased from the previous zone, while Cyperaceae pollen (2.9%) decreased.
Fossil midden DCA
The first two axes of the DCA performed on the fossil midden samples is shown in Figure 6. The first DCA axis had an eigenvalue of 0.3129, and a length of 2.3642 SD. The second DCA axis had an eigenvalue of 0.2203, and the axis length was 2.5927 SD. Modern samples and submodern samples (114–107 cal yr BP) from Zone B2 clustered together near positive values on DCA axis 1. The older samples (Zones A2, A1, and B1) clustered near negative values on DCA axis 1.
Detrended correspondence analysis (DCA) of fossil middens. Samples are coded by quantitatively determined pollen zone.
Fossil midden stable isotopes
Bulk δ15N values showed a gradual depletion over time (r = −0.7210) from 4038 cal yr BP (10.9‰) to present (5.4‰ average). In contrast, bulk δ13C values did not show a clear trend. Averages of bulk δ13C in each pollen zone show they remained relatively consistent (−26.2 to −25.5‰), until an approximately 2‰ depletion in the modern samples (−27.2‰). δ18O from the speleothem records versus δ15N from the middens demonstrated a negative correlation (r = −0.7051), wherein more depleted values of δ18O (−1.1‰) corresponded with more enriched values of δ15N (10.9‰). The linear regression explained 49.71% of the variance in the δ15N data (Fig. 7).
(A) The δ15N values of the middens plotted by age in calibrated years BP. (B) The average speleothem δ18O plotted against midden N. (C) A plot of the bulk δ13C values by midden age in calibrated years BP. (D) A box plot of midden δ13C values by age bin.
DISCUSSION
Hyrax midden pollen and modern vegetation
The pollen data from the modern hyrax middens were closely aligned with documented vegetation in each ecological zone and thus captured a local signal of vegetation (Table 1). On the coastal plain, Poaceae (18.92%), Dracaena (31.01%), and Senegalia III (6.81%) are most abundant. The vegetation in this region has been significantly reduced due to overgrazing by domesticated animals and other human activity, resulting in a desert grassland with sparse Senegalia tortilis trees (Miller and Morris, Reference Miller and Morris1988). In the escarpment samples, Poaceae (67.6%) and T. dhofarica (7.4%) were found in high pollen abundance. Suaeda (6.3%) is common among coastal vegetation communities, and the escarpment samples come from the southernmost area nearest the coastal plain (Miller and Morris, Reference Miller and Morris1988; Patzelt, Reference Patzelt2015; Fig. 1). One of these samples contained 12.1% T. dhofarica pollen. These samples were camel dung and therefore indicate direct consumption, introducing a dietary bias that created larger pollen abundances than those that result from eolian deposition (Scott and Cooremans, Reference Scott and Cooremans1992). While there is likely dietary contribution of pollen into the hyrax middens, this camel dung was collected from an animal actively browsing on the escarpment and on T. dhofarica plants. The pollen abundances in these samples can be used as a tentative benchmark for what could be expected for high dietary input of T. dhofarica pollen in the hyrax middens (Scott and Cooremans, Reference Scott and Cooremans1992; Gil-Romera et al., Reference Gil-Romera, Lamb, Turton, Sevilla-Callejo and Umer2010; Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012). Terminalia dhofarica is limited to the escarpment woodlands today (Miller and Morris, Reference Miller and Morris1988; Hildebrandt et al., Reference Hildebrandt, Al Aufi, Amerjeed, Shammas and Eltahir2007 Patzelt, Reference Patzelt2015).
The distal plateau samples are dominated by the tree taxa S. persica (17.7%) as well as Poaceae (9.2%) pollen. The plateau ecological zone is a grassland with sparse trees (Miller and Morris, Reference Miller and Morris1988). Salvadora persica is found along wadi drainage systems, preferring wetter soils (Miller and Morris, Reference Miller and Morris1988). Boswellia sacra (frankincense) is higher in abundance in the distal plateau samples (6.5%), which is this plant's preferred habitat (Miller and Morris, Reference Miller and Morris1988; Patzelt, Reference Patzelt2015). All the Nejd samples contain high abundances of Senegalia III (7.2–9.7%). Senegalia vegetation communities are prolific throughout the desert of Dhofar (Miller and Morris, Reference Miller and Morris1988; Ghazanfar, Reference Ghazanfar2004). Modern samples from east Nejd have a significant contribution from the pollen taxa Polycarpon-type (Reseda) (39.2%). A member of the genus Reseda, R. sphenocleoides, is common in the dry wadi drainage systems of the Nejd (Raffaelli et al., Reference Raffaelli, Mosti and Tardelli2003). Cyperaceae pollen is found in a higher proportion in the west Nejd (7.8%). Generally, sedges found in the inland desert are members of the genus Cyperus, particularly Cyperus conglomeratus, which is found even among the sand dunes of the Rub al’ Khali Desert, or the Empty Quarter (Miller and Morris, Reference Miller and Morris1988). Semi-aquatic varieties of Cyperaceae are found on the coast, typically near estuaries (Miller and Morris, Reference Miller and Morris1988; Hoorn and Cremaschi, Reference Hoorn and Cremaschi2004).
The CONISS results for the samples presented distinguished all the modern Nejd samples, which cover a wide geographic area, from the submodern samples (160–110 cal yr BP). Additionally, the CONISS results distinguished all other samples by geographic location (and ecological zone). The DCA of the modern samples illustrates this ecological gradient, where samples cluster near taxa that today are abundant in their respective ecological zones. These statistical analyses suggest that middens preserve a pollen signal of the local vegetation within a reasonable degree of reliability (Figs. 3 and 4).
Fossil pollen interpretation
We interpret the dated middens as averaged time slices representing approximately decades to ~100 yr of deposition. The fossil pollen record reveals variability between samples of similar ages. While the samples come from the same wadi drainage system, there is still some geographic distance between sample sites (~0.25–4.4 km). Variability in their pollen compositions may reflect the vegetation in the immediate vicinity outside the caves as well as dietary biases from hyrax foraging (Scott and Woodborne, Reference Scott and Woodborne2007; Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012; Ivory et al., Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021). Having a higher sample density of middens with similar ages but from slightly disparate locations thus gives a broader picture of the vegetation in the east Nejd at a particular time. Moreover, it is important to note that despite the dissimilarities between samples of similar ages, the CONISS statistical analysis reveals that their overall compositions are most similar to one another in comparison to all other samples.
The fossil pollen record demonstrates a change in the vegetation communities such that arboreal taxa with mesic affiliations on the modern landscape (i.e., Combretaceae, Maytenus) were more prevalent ~4000–3000 cal yr BP. After 1500 cal yr BP, more xeric taxa (i.e., Senegalia, Kohautia) became more abundant, and the density of vegetation was much sparser (Figs. 5 and 8). In the DCA, samples grouped near pollen taxa that characterized their composition, which captured this ecological gradient through time along the first axis (McCune and Grace, Reference McCune and Grace2002; Fig. 6). Taxa associated with the Nejd today, such as Senegalia III, S. persica, and Poaceae were on the positive side of DCA axis 1 near the modern and submodern samples (~120–100 cal yr BP). Emblematic taxa of the older groups were Boscia/Cadaba and the Combretaceae family (mainly Terminalia), neither of which exist in the Nejd today (Patzelt, Reference Patzelt2015).
(A) Archaeological periods of monument building and settlement, along with the earliest evidence for the introduction of domesticated camels in Dhofar (2000 yr BP) and elsewhere in Arabia (3000 yr BP). (B) Mesic taxa relative abundances (%): Ficus, Boswellia sacra, Boscia/Cadaba, Maytenus. (C) Nejd association relative abundances (%): Amaranthaceae, Salvadora persica, Senegalia I, Senegalia III, Commiphora. (D) Grazing indicator relative abundances (%): Dodonaea viscosa-type, Cornulaca/Aerva, Cassia-type, Heliotropium. (E) Gray bars showing Sporormiella relative abundance (%) and black line indicating microcharcoal concentrations (particles/g). (F) Speleothem δ18O from Fleitmann et al. (Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007).
In the early part of the pollen record (4038–2920 cal yr BP), there was a higher proportion of tree pollen taxa (~20–57%) on the landscape relative to herbaceous taxa (0–16%). Trees such as Boscia/Cadaba and Ficus were more abundant on average until approximately 3000 cal yr BP. These trees are common on the landscape today but are typically found in moister places (Miller and Morris, Reference Miller and Morris1988; Patzelt, Reference Patzelt2015). There was also a high abundance of Combretaceae pollen in the sample dated to 3100 cal yr BP. Although multiple members of this family are found throughout the Afrotropics, only T. dhofarica is native to Dhofar (Miller and Morris, Reference Miller and Morris1988; Patzelt, Reference Patzelt2015). This makes T. dhofarica the most likely candidate to have been present during this interval. Terminalia dhofarica is an insect-pollinated plant group often underrepresented in pollen spectra. Although no modern middens were found in Terminalia woodland, limiting our ability to examine the representativity of its pollen in middens, abundances of T. dhofarica from within fresh camel dung collected during browsing on an individual tree resulted in values of 12.1%. To the extent that these samples can be used to benchmark the data from the hyrax middens, we tentatively interpret the even higher values in this fossil sample of >30% to indicate a local presence of this tree in the east Nejd at ~3100 cal yr BP (Miller and Morris, Reference Miller and Morris1988; Lippi et al., Reference Lippi, Gonnelli and Raffaelli2007; Oberprieler et al., Reference Oberprieler, Meister, Schneider and Kilian2009; Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012).
The sample at 3100 cal yr BP also contained high abundances (39.9%) of other mesic tree taxa, including Boscia/Cadaba-type. This supports the idea that during the period of deposition of this sample, woodlands more like those currently growing in the modern escarpment were supported in the Nejd. Further, this sample had a high concentration of microcharcoal (36,605 particles/g) (Fig. 8). Modern vegetation in the Nejd is severely fuel-limited due to the sparseness of the vegetation. The presence of increased charcoal suggests that vegetation during this interval was continuous enough to be more conducive to burning (Blackford, Reference Blackford2000; Chase et al., Reference Chase, Meadows, Scott, Thomas, Marais, Sealy and Reimer2009; Genet et al., Reference Genet, Daniau, Mouillot, Hanquiez, Schmidt, David and Georget2021).
Though paleoecological records in this region are fragmentary, several suggest wetter conditions in coastal southern Arabia and more pervasive woodlands in the desert of Yemen ~10–4 ka (Lézine et al., Reference Lézine, Saliège, Mathieu, Tagliatela, Mery, Charpentier and Cleuziou2002; Parker et al., Reference Parker, Goudie, Stokes, White, Hodson, Manning and Kennet2006; Fleitmann et al., Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007; Ivory et al., Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021). Speleothem δ18O from Qunf Cave indicates higher precipitation starting at ~10 ka, which then began to decrease around 8–7 ka until the present (Fleitmann et al., Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007). Sedimentological and pollen evidence from the United Arab Emirates illustrates the presence of interdunal lakes during a wetter Early Holocene, which became desiccated by the Late Holocene at ~4000 cal yr BP and a C4 dominated plant community became established (Parker et al., Reference Parker, Eckersley, Smith, Goudie, Stokes, Ward, White and Hodson2004, Reference Parker, Goudie, Stokes, White, Hodson, Manning and Kennet2006). Pollen records from coastal estuaries demonstrate changes mainly in wetland and mangrove taxa; however, they provide some evidence that communities farther inland included tropical taxa from ~6000 to 4500 cal yr BP (Lézine et al., Reference Lézine, Saliège, Mathieu, Tagliatela, Mery, Charpentier and Cleuziou2002). Pollen from hyrax middens in Yemen indicate a diverse, semiarid woodland farther inland in the modern-day desert at Wadi Sana during the mid-Holocene (6–4.7 ka), with high local abundances of Terminalia (Ivory et al., Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021). The pollen data presented here complement these records, suggesting a denser arboreal community was present in the Nejd in Dhofar from ~4000 to 3000 cal yr BP.
After the gap in the hyrax midden record (~1500 cal yr BP), the composition of the vegetation communities was much different. Between ~2900 and 1500 cal yr BP, there was a taxonomic turnover characterized by a pronounced increase in herbaceous pollen taxa (Amaranthaceae and Poaceae) and tree pollen taxa (Senegalia III and S. persica) indicative of modern Nejd communities (Fig. 8). Species of Senegalia are widespread in Dhofar but are most common in the Nejd and make up most of the trees in this zone (Miller and Morris, Reference Miller and Morris1988). The herbaceous Amaranthaceae family is also dominant in this part of the record. Many of the species of Amaranthaceae in Dhofar are weeds in cultivated areas or grow on disturbed ground, as well as in xeric environments (Miller and Morris, Reference Miller and Morris1988). Additionally, after 1500 cal yr BP, microcharcoal concentrations were much lower (94.9 particles/g). This decrease in charcoal in combination with indications of xeric vegetation suggests a change in fire dynamics to a regime more like the modern day with less fuel for natural wildfires (Fig. 8).
Monsoon dynamics and aridity
Regional paleoclimate records suggest a gradual decrease in rainfall across the Holocene in southern Arabia. The mechanism behind this decline has traditionally been interpreted as the southward migration of the Intertropical Convergence Zone (ITCZ) following decreasing Northern Hemisphere summer insolation during the mid-Holocene (Fleitmann et al., Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007; Lézine et al., Reference Lézine, Bassinot and Peterschmitt2014; Nicholson, Reference Nicholson2018). More recently, climatologists suggest that this latitudinal shift in the rain belt is driven by the development of the African Westerly Jet and subsequent movement of the African Easterly Jet (Nicholson, Reference Nicholson2009). Moreover, the vertical rising of the ITCZ over the ocean amplifies this effect by widening the rain belt and increasing the duration of the rainy season (Nicholson, Reference Nicholson2009). These two processes lead to the intensification of the summer monsoon over land. The speleothem δ18O records from Dhofar suggest the variation in rainfall over this time are related to changes in Northern Hemisphere insolation (Fleitmann et al., Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007).
The presence of T. dhofarica in the Nejd at 3100 cal yr BP and the high abundances of other relatively mesic taxa (e.g., Boscia/Cadaba) suggest that the range of semiarid woodlands was more expansive in the early part of the Late Holocene (4000–3000 cal yr BP). These taxa were locally abundant in the Nejd at this time, at least 25–30 km farther inland than their modern extent. A stronger monsoon during this interval would have brought increased precipitation and/or fog and likely supported more arboreal vegetation farther inland than today (Ivory et al., Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021). While fog is an important climatic factor for modern woodland vegetation in the region, speleothem oxygen isotopes provide a record of rainfall; they do not provide direct information about fog (Fleitmann et al., Reference Fleitmann, Burns, Neff, Mudelsee, Mangini and Matter2004, Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007). Speleothem growth occurs when water seeps into a cave, and in Dhofar this is strongly tied to the summer monsoon, which brings in both fog and rainfall (Fleitmann et al., Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007). Thus, speleothem δ18O is an indicator of this moisture source rather than rainfall or fog alone. Regardless, pollen evidence suggests more expansive semiarid woodlands than seen today.
Additionally, although the hyrax midden record only provides snapshots of vegetation from collected intervals, there is evidence of some level of resilience of woodland taxa to increasing aridification during the Late Holocene. For example, T. dhofarica was locally present in the desert at 3100 cal yr BP, ~3000–4000 yr after the onset of decreasing precipitation regionally (Fleitmann et al., Reference Fleitmann, Burns, Neff, Mudelsee, Mangini and Matter2004; Lézine et al., Reference Lézine2007). Transient climate model simulations indicate that there were abrupt changes in rainfall as the ITCZ retreated southward and the monsoon weakened (Lézine et al., Reference Lézine, Ivory, Braconnot and Marti2017). These model results, compared with mangrove pollen data from the coast, suggest an abrupt decrease in rainfall at 4000 cal yr BP (Lézine et al., Reference Lézine, Saliège, Mathieu, Tagliatela, Mery, Charpentier and Cleuziou2002, Reference Lézine, Ivory, Braconnot and Marti2017). In the early part of the record, the mangroves contained pollen of Rhizophora, a coastal, brackish taxon that requires some freshwater input (Lézine et al., Reference Lézine, Ivory, Braconnot and Marti2017), which became extremely rare after ~4000 cal yr BP and was replaced by more saline- and drought-tolerant species (Lézine et al., Reference Lézine, Saliège, Mathieu, Tagliatela, Mery, Charpentier and Cleuziou2002). This suggests a transition to more arid conditions in Oman (Lézine et al., Reference Lézine, Ivory, Braconnot and Marti2017). However, the arboreal community farther north in the east Nejd persisted for another ~1000 yr after this transition, suggesting a resilience to increasing aridity in the Late Holocene.
The gap in the hyrax midden record from 2920 cal yr BP to 1651 cal yr BP is coeval with a hiatus in the Qunf Cave speleothem record (Fleitmann et al., Reference Fleitmann, Burns, Neff, Mudelsee, Mangini and Matter2004). Regional paleoclimate records from Arabia, Africa, and western Asia indicate this was an especially dry period, and it may be that the interior Nejd did not have enough food and water resources to sustain a hyrax population during this period (Gasse and Van Campo, Reference Gasse and Van Campo1994; Fleitmann et al., Reference Fleitmann, Burns, Neff, Mudelsee, Mangini and Matter2004; Ivory and Lézine, Reference Ivory and Lézine2009; Gil-Romera et al., Reference Gil-Romera, Lamb, Turton, Sevilla-Callejo and Umer2010). Hyraxes obtain most of their water from foraged vegetation, especially in arid regions (Sale, Reference Sale1965; Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012; Mohamed, Reference Mohamed2019). When drought conditions occur and herbaceous plants do not grow or desiccate on the landscape, the trees become a critical source of both food and water (Sale, Reference Sale1965). Hyraxes have even been observed stripping bark from trees such as Senegalia in southern Africa when under severe drought stress (Sale, Reference Sale1965). The reduction of the trees during this interval, as seen in the shift in vegetation once middens are again deposited, suggests that hyraxes may have lacked these necessary resources during this arid interval. The alternative hypothesis would be that this gap is simply the result of insufficient sampling. While this is certainly possible, there are many independent lines of evidence indicating that the Nejd may have been too dry and resource depleted during this interval. Additionally, the middens that are dated to ~1500 cal yr BP after this hiatus co-occur with the redeposition of speleothems at Qunf Cave as well as an observed wet phase in the coastal estuaries (Hoorn and Cremaschi, Reference Hoorn and Cremaschi2004; Fleitmann et al., Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007).
Bulk δ15N data from hyrax middens have previously been interpreted to indicate local changes in moisture availability. Soil and plant foliar δ15N have an established inverse relationship with water availability that has also been demonstrated in herbivore feces (Chase et al., Reference Chase, Scott, Meadows, Gil-Romera, Boom, Carr, Reimer, Truc, Valsecchi and Quick2012; Wang et al., Reference Wang, Wang, Liu, Wu, Lü, Fang and Cheng2014; Carr et al., Reference Carr, Chase, Boom and Medina-Sanchez2016; Díaz et al., Reference Díaz, Frugone, Gutiérrez and Latorre2016). δ15N is also negatively correlated with MAP globally (Wang et al., Reference Wang, Wang, Liu, Wu, Lü, Fang and Cheng2014). In our record, δ15N became more depleted over time, which would counterintuitively suggest increasing water availability over this study interval. In contrast, all other evidence, from regional precipitation records to the change in vegetation in this area, strongly indicates drying (deMenocal et al., Reference deMenocal, Ortiz, Guilderson, Adkins, Sarnthein, Baker and Yarusinsky2000; Fleitmann et al., Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007; Lézine et al., Reference Lézine, Ivory, Braconnot and Marti2017; Ivory et al., Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021). However, the inverse relationship between water availability and δ15N observed in previous studies may not apply in hyperarid regions.
A study by Díaz et al. (Reference Díaz, Frugone, Gutiérrez and Latorre2016) looked at plants and herbivore feces δ15N across an aridity gradient in the Atacama Desert. They observed a unimodal relationship between herbivore fecal δ15N and moisture availability. Wang et al. (Reference Wang, Wang, Liu, Wu, Lü, Fang and Cheng2014) observed this same curve across an aridity gradient in savannah grassland in both soil δ15N and plant foliar δ15N. Likewise, this study demonstrated a positive correlation between soil and plant δ15N and MAP at an arid location. This suggests that after a certain threshold, different controls on the nitrogen cycle become more dominant, such as loss of gaseous nitrogen or nitrogen fixation by bacteria (Wang et al., Reference Wang, Wang, Liu, Wu, Lü, Fang and Cheng2014). The inverse relationship between hyrax midden bulk δ15N and speleothem δ18O from this study implies a positive correlation between bulk δ15N and MAP in Dhofar, and thus continued aridification, over the last 4000 yr (Fig. 7).
Human–environment interactions
Archaeological evidence attests to the movement of ancient pastoralists across the Dhofar region (Harrower et al., Reference Harrower, Senn and McCorriston2014; McCorriston et al., Reference McCorriston, Harrower, Steimer, Williams and Senn2014, Reference McCorriston, Moritz, Buffington, Pustovoytov, Ivory, Abuazizeh, Purdue, Charbonnier and Khalidi2018, Reference McCorriston, Buffington, Olson, Martin, Abuazizeh, Everhart, Al Maashani, Al Kathiri and Al Mehri2020). Generally, there is sparse evidence for prolonged habitation in any one spot, suggesting pastoralists were highly mobile (McCorriston et al., Reference McCorriston, Moritz, Buffington, Pustovoytov, Ivory, Abuazizeh, Purdue, Charbonnier and Khalidi2018). Small monuments were constructed across Dhofar over the last 7000 yr (McCorriston et al., Reference McCorriston, Harrower, Steimer, Williams and Senn2014, Reference McCorriston, Moritz, Buffington, Pustovoytov, Ivory, Abuazizeh, Purdue, Charbonnier and Khalidi2018). This was punctuated by one period of visible settlement by cattle herders on the plateau at ~2 ka, where there are permanent structures documenting ~200 yr of abandonment and reoccupation (McCorriston et al., Reference McCorriston, Moritz, Buffington, Pustovoytov, Ivory, Abuazizeh, Purdue, Charbonnier and Khalidi2018, Reference McCorriston, Buffington, Olson, Martin, Abuazizeh, Everhart, Al Maashani, Al Kathiri and Al Mehri2020). These sites were near more stable water sources, but there is no evidence for the development of settled agriculture (McCorriston et al., Reference McCorriston, Buffington, Olson, Martin, Abuazizeh, Everhart, Al Maashani, Al Kathiri and Al Mehri2020).
Historically, there has been a lack of understanding regarding how pastoralist practices impact vegetation, and past theoretical frameworks often focused on exploitation and depletion of habitat resources (i.e., the “tragedy of the commons”) (Hardin, Reference Hardin1968; Warren, Reference Warren1995). However, recent studies have demonstrated the sustainability of pastoralism even under increasing aridity (Brierley et al., Reference Brierley, Manning and Maslin2018). Linking paleoecological records with archaeological data allows for an increased understanding of long-term human–environment interactions in pastoralist systems. In the early part of the hyrax midden pollen record, there is evidence for more continuous arboreal vegetation cover, and archaeological evidence suggests mobility of pastoralist groups until ~2350 cal yr BP (Harrower et al., Reference Harrower, Senn and McCorriston2014; McCorriston et al., Reference McCorriston, Moritz, Buffington, Pustovoytov, Ivory, Abuazizeh, Purdue, Charbonnier and Khalidi2018). Mesic trees were present farther inland in the Nejd even after 3000–4000 cal yr BP of drying and 4000 yr of a mobile herding practice in Dhofar. This suggests that pastoralists did not degrade woodland vegetation at this time.
Beginning around 1000 cal yr BP, there was a pronounced increase in grazing indicator pollen taxa (12.5%). Likewise, at approximately 500 cal yr BP, there was an increase in the abundance of Sporormiella (1.9–2.3%), a fungus found in the dung of large herbivores, which in Dhofar is found abundantly in camel dung (Ivory et al., Reference Ivory, Cole, Anderson, Anderson, McCorriston and Williams2021). The observation of Sporormiella in the middens likely occurs through hyraxes walking across soil where camels are present, as the fungus would be trapped in the dung that is on the ground, as well as eolian transport. The increase in grazing indicator taxa and Sporormiella may indicate an intensification of land use in the inland desert, particularly camel herding, beginning at 1000–500 cal yr BP. While the distribution of grazing indicator taxa would have also been influenced independently by other ecological or climatic controls, the combination of the higher abundances of these particular pollen taxa and Sporormiella point to an increase in domesticated herbivores on the landscape. These pollen taxa are low in abundance in the earlier part of the record (6.6%), suggesting that animal grazing on the vegetation would have been relatively low until ~1000 cal yr BP.
In the modern cloud forests on the escarpment, higher stocking rates of camels increase the abundance of unpalatable plant species, or grazing indicators, and decrease plant diversity (Ball and Tzanopoulos, Reference Ball and Tzanopoulos2020). Preferential grazing of the softer shoots and saplings of T. dhofarica by camels is already being shown to affect the regeneration of these key trees (Ball and Tzanopoulos, Reference Ball and Tzanopoulos2020). Maintaining these high browsing pressures under anthropogenic climate change may ultimately lead to the degradation of the cloud forest (El-Sheikh, Reference El-Sheikh2013; Ball and Tzanopoulos, Reference Ball and Tzanopoulos2020). However, it is important to note the long-term sustainability of pastoralism under lower stocking rates, as shown through the archaeological record and the paleoecological evidence presented here. The earliest evidence for domesticated camel herding in Dhofar is from 2 ka, but there is no observable increase in grazing indicators or Sporormiella for another 500 to 1000 yr in the collection region of our samples (McCorriston et al., Reference McCorriston, Moritz, Buffington, Pustovoytov, Ivory, Abuazizeh, Purdue, Charbonnier and Khalidi2018).
CONCLUSION
The pollen data from the rock hyrax midden record demonstrate a turnover from a more mesic, arboreal vegetation community to the more xeric community that characterizes the Nejd today. While the nature of the termination of the Holocene Humid Period is debated, an arboreal community persisted in the Nejd for approximately 4000–3000 cal yr BP after the onset of decreasing rainfall (Fleitmann et al., Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007). Bulk stable isotope data from the middens indicate a transition to hyperaridity over this time frame. These combined data suggest some resilience of this biodiverse dryland community under increasingly arid conditions. The end of the hiatus in the midden record and its co-occurrence with the renewal of speleothem growth and increased runoff at the coast suggest this overall trend was perhaps punctuated by a wetter phase beginning at ~1500 cal yr BP (Hoorn and Cremaschi, Reference Hoorn and Cremaschi2004; Fleitmann et al., Reference Fleitmann, Burns, Mangini, Mudelsee, Kramers, Villa and Neff2007).
Modern human land use enhances the risk of vegetation degradation, and anthropogenic climate change is likely to push this region into novel climate spaces (Dahinden et al., Reference Dahinden, Fischer and Knutti2017; Ball and Tzanopoulos, Reference Ball and Tzanopoulos2020). There is an outstanding need to mitigate the effects of global climate change and reduce degradational impacts from human land use to help maintain this biodiverse and vulnerable vegetation community. Evidence for the practice of nomadic pastoralism in southern Arabia dates to at least 7000 cal yr BP (Martin and Roe, Reference Martin, Roe, McCorriston and Harrower2020). Indicators of more intense human landscape use do not appear in the paleoecological record generated from the middens until 1000–500 yr BP. The lack of evidence for human impacts on vegetation for the bulk of the record highlights continued sustainability of pastoralism in this region under changing climate conditions. In terms of vegetation composition, the modern samples were considerably different compared with the fossil samples, indicating the recent economic growth and substantially higher stocking rates are an unprecedented driver of vegetation change in Dhofar. It is important to consider the context provided by these long-term records when discussing human activity and impacts to the landscape: although animal grazing may be degradational to the modern vegetation, it has not always been in the past, and there may be conservation options that preserve the practice of nomadic pastoralism in Dhofar and other drylands.
Supplementary material
The supplementary material for this article can be found at https://doi.org/10.1017/qua.2023.42
Acknowledgments
This work was supported by NSF-CNH (1617185) for fieldwork and pollen analysis. Additional support was provided through the RJ Cuffey Fund for Paleontology and the Michael Loudin Family Graduate Scholarship through the Department of Geosciences at Penn State University. The authors sincerely thank our colleagues with the Oman Ministry of Heritage and Tourism under His Majesty Sultan Haitham Bin Tariq Al Said for contributions in the field and for their hospitality to our team while abroad. We also thank the Oman Botanic Garden, as well as Annette Patzelt and Darach Lupton, for their assistance with modern plant identification. We are grateful to the Ancient Socio-ecological Systems of Oman (ASOM) team for their unending support. We would also like to acknowledge the contributions made to this project by Kenneth Cole, who tragically passed away during the writing process.
Open access
