Late Holocene wetland transgression and 500 years of vegetation and fire variability in the semi-arid Amboseli landscape, southern Kenya
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The semi-arid Amboseli landscape, southern Kenya, is characterised by intermittent groundwater-fed wetlands that form sedimentary geoarchives recording past ecosystem changes. We present a 5000-year environmental history of a radiocarbon dated sediment core from Esambu Swamp adjacent to Amboseli National Park. Although radiocarbon dates suggest an unconformity or sedimentary gap that spans between 3800 and 500 cal year BP, the record provides a unique insight into the long-term ecosystem history and wetland processes, particularly the past 500 years. Climatic shifts, fire activity and recent anthropogenic activity drive changes in ecosystem composition. Prior to 3800 cal year BP the pollen data suggest semi-arid savanna ecosystem persisted near the wetland. The wetland transgressed at some time between 3800 and 500 cal year BP and it is difficult to constrain this timing further, and palustrine peaty sediments have accumulated since 400 cal year BP. Increased abundance of Afromontane forest taxa from adjacent highlands of Kilimanjaro and the Chyulu Hills and local arboreal taxa reflect changes in regional moisture budgets. Particularly transformative changes occurred in the last five centuries, associated with increased local biomass burning coeval with the arrival of Maa-speaking pastoralists and intensification of the ivory trade. Cereal crops occurred consistently from around 300 cal year BP, indicative of further anthropogenic activity. The study provides unique insight in Amboseli ecosystem history and the link between ecosystem drivers of change. Such long-term perspectives are crucial for future climate change and associated livelihood impacts, so that suitable responses to ensure sustainable management practices can be developed in an important conservation landscape.
KeywordsAmboseli Charcoal Environmental history Pollen Savanna Swamps
Rapid ecosystem changes, particularly during the recent past, are primarily attributed to anthropogenic modifications that are superimposed on long-term climatic and landscape-scale changes (Young 2014). East African savannas support large human (Lane 2013) and herbivore (Sarkar 2006) populations and are currently undergoing rapid development and pressure on water resources (Bond and Midgley 2000; Thenya 2001). These changes are leading to wildlife habitat degradation and fragmentation (Moses et al. 2016), biodiversity loss (Western and Maitumo 2004; Muchiru et al. 2009), and other stressors surrounding the community conservation nexus. To understand, and uncouple, how these abiotic and biotic factors interact it is crucial to have a long-term perspective on ecosystem change that can be used to understand how entangled interactions between the environment, ecosystems and humans influence the current state of the ecosystem and possible future trajectories (Marchant and Lane 2014).
Reconstructing the vegetation, climate and fire dynamics is of particular interest as the Amboseli landscape supports migratory wildlife that move between the Kenyan and Tanzanian border. An understanding of the response of the remaining Amboseli wetlands to changes in driving factors such as climate change, wildlife use, fire and anthropogenic factors over time is necessary to inform sustainable wetland management of the wetlands that are important dry season grazing refuges for wildlife. There have been relatively few palaeoecological studies in southern Kenya due to the extensive coverage of semi-arid savanna ecosystems, woodland and scrub vegetation with limited suitable sedimentary basins providing few localised records (Rucina et al. 2010). We present pollen, non-pollen palynomorph and macroscopic charcoal data providing insights into the evolution of the wetland and the interaction of fire, vegetation and climate within the Amboseli ecosystem.
Climate and geologic setting
The Amboseli landscape (Fig. 1) is characterised by five main components: gently undulating basement plains on deep, acidic, well-drained soils; palaeolacustrine basin and swamps; basal slopes of Kilimanjaro with deep, well-drained neutral soils; volcanic landscapes with abundant small to block sized volcanic cones, reddish brown scoria pyroclasts and shallower soils that support semi-arid woodland and scrub; and denser woodland savanna on young basaltic parent material toward Chyulu Hills.
Vegetation in the region is characterised by sparse shrubland savanna and Acacia-Commiphora dominated dry woodland-lowland savanna. Throughout this paper, we use Acacia to describe African acacias of Vachellia and Senegalia genera. Crosscutting these landscapes are riparian wooded areas following semi-permanent and seasonal channels draining northward from Kilimanjaro and then eastward to converge with the Galana River catchment to Tsavo.
Recent land use changes across the Amboseli area
Land cover changes, notably between open savanna and woody savanna, have been quite common across Africa in response to indirect and direct human activities and climatic changes (Gillson and Marchant 2014). In North Pare, Tanzania, an increase in tree cover after the 19th century was noted after British colonial land use policies encouraged agroforestry to meet timber demand leading to the increased planting of exotic species such as Eucalyptus (Gillson 2004). In Amboseli, control of the movement of elephants has been proven to drive woodland density (Western and Maitumo 2004) with high elephant numbers causing a loss in woodland. There have been rapid ecosystem changes to the Amboseli area over the past 100 years caused by animal disease outbreaks, agricultural expansion, watercourse diversion, reduction of tree cover, and water extraction from the wetlands outside of protected areas (MEMR 2012). There is increasing concern regarding the management of the area due to competition for water resources by humans and wildlife, global temperature increases, the notable decrease in rainfall on Kilimanjaro that has reduced ~ 36% since 1910 and the extensive loss of cloud forests (Hemp 2005). The hydrological loss from the destruction of montane and cloud forests on Kilimanjaro is greater than that of the glaciers retreat (Hemp 2005). Recently, the wider Amboseli landscape experienced major droughts in 1984, 1994 and 2008–2009 that have emphasised the need for multi-stakeholder conservation and management of wetlands due to rapid increases in human population and associated land use pressures (MEMR 2012). A 10-year management plan was developed through participation between Amboseli Basin stakeholders that builds on the previous management plan (1991–1996) (Kenya Wildlife Service 2008).
Pastoralist populations with historical formal and informal land tenure have recently reorganised into more sedentary group ranches whereby some groups and individuals maintain pastoral livelihoods on an increasingly fragmented socio-ecological landscape. People have migrated into the region and the increased population have placed additional demand on the Amboseli wetlands (Sarkar 2006). Land cover and land uses include commercial agriculture, particularly expansive in and around the wetlands, pastoralism across the landscape, rural urbanisation, and various protected areas including National Parks, community and private game reserves.
Materials and methods
A 247.5-cm core was collected in 2009 at − 2.711913, 37.554357 (1191 m a.sl.) using a Russian corer with a 5-cm-diameter, 50-cm-long, hemi-cylindrical collection chamber from proximal, overlapping (~ 10 cm), parallel boreholes through 10 cm of standing water. Cores sections were wrapped in aluminium foil and transferred to split plastic PVC pipes for transport and refrigeration at the Palynology and Palaeobotany Section, National Museums of Kenya (NMK), Nairobi. Subsamples were extracted for pollen analysis at NMK and subsamples sent to the University of York, UK, for charcoal analysis.
Geochronology and age-depth modelling
One Acacia sp. wood fragment and five bulk organic sediment subsamples were accelerator mass spectroscopy (AMS) radiocarbon dated. Samples sent to the 14CHRONO laboratory (Queen’s University Belfast, Northern Ireland) were acid wash pre-treated prior to combustion to CO2, graphitization and AMS using a NEC 0.5 MV compact accelerator (Reimer 2015). Samples sent to Direct AMS (Bothell, WA, USA) were acid–base–acid washed, combusted, graphitized and measured using a National Electrostatics Corporation (NEC) 1.5 SDH Compact Pelletron 500 kV accelerator mass spectrometer. Reported dates were corrected for instrumental isotopic fractionation 13C values by the respective laboratories. Radiocarbon dates were calibrated using the IntCal13 curve (Reimer et al. 2013) and used to build a linear interpolated age-depth model using the R script Clam version 2.2 (Blaauw 2010) for the upper palustrine peaty sediments. Lower sediments were not age-depth modelled and the radiocarbon dates were used to examine the maximal time interval that represented wetland transgression, a sediment gap and potential unconformities. This information provides palaeoenvironmental context for the history of the site. Henceforth, we refer to all calibrated ages as years before present (year BP), CE 1950 (Common Era).
Pollen and palynomorph analysis
Sediment cores were subsampled for 1 cm3 of wet sediment taken from 100 depths at 2.5-cm intervals down the core and pollen and non-pollen palynomorphs (NPP) were isolated using sequential chemical digestion (Fægri and Iversen 1989). Pollen identification was performed on 70 levels using ×400 and ×1000 magnification to a minimum count of 350 grains. The other 30 pollen samples were left out due to low pollen numbers (> 350). Pollen identifications were made with the aid of the pollen reference collection at the Palynology and Palaeobotany Section, NMK, Nairobi. Relative abundances were calculated from the terrestrial pollen sum and aquatic taxa relative abundances were calculated from the aquatic taxa sum of Cyperaceae, Hydrocotyle, Myriophyllum, Nymphaea and Typha. NPP, including fungal spores, were identified from 100 levels with the aid of a taxonomic key (van Geel et al. 2011) and the relative abundances of spore types were calculated using the total NPP sum per sample.
Macroscopic charcoal analysis
A total of 125 subsamples of 1 cm3 were collected at intervals of between 1 and 5 cm. To each subsample, sodium hexametaphosphate and distilled water were added to disaggregate the samples and aid in separation of organic material and clays. Samples were then washed through a 125-μm sieve and the retained charcoal particles tallied under a Zeiss Stemi 2000-C stereomicroscope between 10 and ×50 magnification and charcoal concentrations were converted to charcoal concentrations (pieces cm−3 of wet sediment) and charcoal accumulation rates (CHAR, pieces cm−2 year1).
Pollen and NPP taxa relative abundances were square-root transformed and CHAR from the same 70 down-core levels were log transformed and included in a principal component analysis (PCA) to examine the correlation structure of the data. Pollen and spore assemblage zones were each identified through constrained hierarchical cluster analysis (CONISS) with the zones being tested for significance using a broken stick test of the sum of squares above the default cut-off implemented with R scripts (R Development Core Team 2015). Pollen taxa were grouped into Afromontane, trees, shrubs, herbs, grasses and aquatics according to their dominant structure at the taxonomic resolution possible through pollen analysis (Table S1).
Illustrative landscape model
The results from the pollen, spore and charcoal analysis, combined with current observations of the wetland landscape, were used to develop a system-wide visual representation of the key components of the wetland and surrounding ecosystem. CONISS zones derived from the pollen spectra defined the time steps but dates have been rounded for graphical representation. Both planar, schematic and cross-sectional views supplemented with example photographs, were created and used to represent the changes in the system over the late Holocene. The relative importance of varying and interacting spatial controls on fire regimes at centennial to millennial temporal scales is represented using a fire regime triangle diagram (Whitlock et al. 2010). Although not set at an absolute scale, the areal extent of the different land use and land cover components portray the relative dominance of the plant group abundance sums from the wetland and the surrounding ecosystems.
Stratigraphy and geochronology
Geochronological determinations of the Esambu palustrine sediment core
F14C ± 1σ error
Collected in 2009
0.9820 ± 0.0028
0.9639 ± 0.0028
0.9522 ± 0.0029
0.6632 ± 0.0024
0.7514 ± 0.0027
0.6077 ± 0.0021
The deepest fine-grained sediments accumulated in a semi-arid savanna ecosystem likely proximal to a wetland from 5000 to approximately 3800 cal year BP. Between 3800 and 500–400 cal year BP the proximal wetland of the Kikarankot River expanded and transgressed the coring site. The data do not permit an examination of the rate of this change or the frequency if there were more than a single transgression. The sediments in this marginal wetland phase may have produced radiocarbon age reversals due to erosion, non-deposition, or bioturbation or physical turbation. An erosional origin resulting from the transition from dominantly semi-arid conditions to increased moisture, or a depositional origin caused by increased aridity with subsequent cessation of sediment accumulation. Due to these uncertainties, we interpret this phase as a marginal wetland transgression leading to the current phase of palustrine peaty sediments that accumulated from 400 cal year BP to present (Fig. 4). Ages prior to 400 cal year BP are estimates based on the radiocarbon ages and potential age-depth models, but uncertainty is lowest from 400 cal year BP to present.
Pollen and NPP assemblage summaries
Pollen zone ESAM 1: 247.5–210.5 cm
Amaranthaceae-Chenopodiaceae and Cyperaceae dominate this zone, with Acacia, Aloe, Asteraceae, Capparis, Poaceae and Tapura consistently present. Acalypha and Juniperus appear towards the top of the zone (Fig. 5). Eighteen spore types are identified in this zone and the charcoal concentration and accumulation rate is relatively low.
Pollen zone ESAM 2a: 210.5–131.5 cm
Cyperaceae, Poaceae, Salvadora and Typha dominate this zone. Diverse arboreal taxa Celtis, Commiphora, Croton, Juniperus, Olea, Podocarpus and Schefflera are also present in this zone. 32 spore types were identified in this zone, and the charcoal concentration and accumulation rate rapidly increase at this level having several charcoal peaks (Fig. 5).
Pollen zone ESAM 2b: 131.5–27.5 cm
Cyperaceae, Poaceae and Typha dominate this zone. Acalypha, Asteraceae, Impatiens and Rhus have a varied presence throughout the zone. Balanites and Celtis appear at 330 cal year BP before disappearing at 200 cal year BP (Fig. 5) from this zone. 27 spore types were identified in this zone. The charcoal concentration and accumulation rate are lower than the previous zone with only two peaks in this zone.
Pollen zone ESAM 2c: 27.5–2.5 cm
Cyperaceae, Poaceae and Typha dominate this zone. Amaranthaceae/Chenopodiaceae, Salvadora and Poaceae grains (> 60 µm) appear consistently throughout this zone with Pinus appearing at four depths since 110 cal year BP. Juniperus, Celtis and Olea are the only Afromontane species that in this zone. 17 spore types are identified in this zone, with Sporormiella occurring consistently (Figs. 5, S2). This zone has very low charcoal concentration levels.
Ecosystem and fire history of the Esambu catchment
The Esambu wetland site is representative of local (≤ 10 km2) vegetation shifts due to its small size (~ 0.4 km2). In addition to this local palaeoenvironmental signal, some Afromontane pollen grains were present, mostly likely derived from the surrounding Chyulu Hills and Kilimanjaro that are indicative of more regional ecosystem changes. A combination of climatic changes, human-herbivore interactions and fires are the key drivers that would have caused the ecosystem to change in composition and distribution. Fires are an important controlling factor within savanna ecosystems and occur regularly with their impact largely controlled by the interaction between climate variability, rates of primary productivity, distribution of fuels, and human land use (Colombaroli et al. 2014). Due to uncertainties with the chronology in the lower part of the core, the ecosystem changes will be presented in three broad periods relating to the mid Holocene, the last two millennia and the last four to five centuries.
From ~ 5000 cal year BP through mid-Holocene, the ecosystem was open patchy savanna dominated by shrubs and trees mainly Amaranthaceae/Chenopodiaceae and Acacia (Fig. 5). Fuels from shrubs and herbs within the Amaranthaceae/Chenopodiaceae landscape are less continuous than more mesic savannas, which support continuous Poaceae-dominated swathes, and are characterised by low-intensity fires (Murphy et al. 2013). Low levels of biomass burning are apparent in the period covered by the mid Holocene Esambu sediments, reflective of the local dry landscape and the pollen record reveals low abundances of herbaceous vegetation and lack of continuous understory. This late Holocene savanna ecosystem was characterised by low fuel connectivity; lack of continuous understory vegetation and abundant woody species means increased areas of open space that act as firebreaks for ground fires.
From the late Holocene to c. 500–400 cal year BP, there is an increase in pollen diversity as the ecosystem surrounding Esambu Swamp became more mesic with an increase in woodland (Commiphora-dominated) and shrub/grassland taxa. Afromontane forest on the adjacent highlands also expanded during this time (Figs. 5 and S2). This local and regional increase in arboreal cover is likely to result from humid and warm conditions manifest as an expansion of Afromontane forest to low altitudes on Kilimanjaro. The period towards c 400 cal year BP has higher charcoal accumulation rates, accompanied by an increase in Afromontane, woody and understory taxa, which we interpret as resulting from increased moisture availability that increased fuel connectivity, and thus increased local burning. Changing pyrodiversity (variation in the overall fire regime) is an important process in grass-dominated ecosystems in Africa, potentially promoting animal and bird richness in mesic savanna areas (Hempson et al. 2017). This signal of increased burning from Amboseli may have been coeval with increased biomass burning reported from the Laikipia Plateau of central Kenya c. 1900–1700 cal year BP (Taylor et al. 2005); this could represent a more regional shift possibly driven by higher precipitation and ensuing biomass cover and fuel connectivity for burning. High spore abundance with Chaetomium, Coniochaeta cf. Ligniaria, Sporormiella, T. HdV-1020 and cf. Valsaria sp. dominating are indicators of high herbivore density (van Geel et al. 2011), as herbivores were concentrated within a relatively small area to access water and grazing from c.800 to 350 cal year BP. This indicates that herbivore densities were high prior to the extreme defaunation that took place during intense ivory trading of the last millennium (Håkansson 2004) driven by European, American and more recently Asian exogenous markets.
After c. 400 cal year BP, when the chronology becomes more secure, the number of Afromontane and woody-shrubland taxa declined. This could have been as a result of human modifications to forest compositions on the mountain slopes, which were cleared in patches and transformed into the mixed agroforestry systems typified by the Chagga home gardens on Kilimanjaro (Hemp 2005) and the Pare Mountains (Finch et al. 2016) of northern Tanzania. This period of marked intensive forest clearance and expansion of sedentary agriculture in the wider region is quite transformative and tied into caravan trades, largely for ivory, and the expansion of New World crop imports such as maize, potatoes and tomatoes. Through this period, there is evidence of highly variable environmental conditions within the Esambu catchment as Typha and Nymphaea decreased and increased; the latter a signal of open water conditions from 400 to 300 cal year BP followed by a drying episode (Fig. 5). Severe droughts lasting decades across equatorial eastern Africa have been observed in historical and sedimentary records (Rourke 2011). The coprophilous spore taxa (Sporormiella) are still consistently present (Fig. 5) suggesting little change in the overall large herbivore density population. However, the source of the dung could have been domesticated species of ungulates (van Geel et al. 2011). Between 400 and 300 cal year BP, mean CHAR values remained low until present, probably because of less plant biomass in the local ecosystem. Current populations near Chyulu Hills apply fire to vegetation cover between May and October (Kamau and Medley 2014) and MODIS satellite observations show relatively few fires in the Esambu area (Fig. 1 inset). The relationship between Sporormiella and Cyperaceae suggests that the density of herbivores at the coring location was higher when Cyperaceae relative abundance increased and aquatic pollen diversity decreased when water level was lower. Aquatic taxa were less abundant but Cyperaceae abundances were maintained by growing in the hydric soils of the moist wetland margin. Currently fires in the Esambu swamp catchment result following human-induced ignition and the spread is driven by limited by fuel abundances, conditions and connectivity. Barren ground patches such as those seen in Fig. 3a limit the spread of fire in many ecosystems (Colombaroli et al. 2014) and grazing intensities can reduce fuel connectivity leading to short-stature lawns, especially during the dry seasons when conditions are more conducive to burning (Archibald et al. 2005).
Disentangling drivers of ecosystem change: insights for management
East African savanna palaeoenvironmental records indicate a highly variable environment from the mid Holocene to present environment (Thompson et al. 2002; Gillson 2004; Rucina et al. 2010). The Esambu pollen record is typical of a semi-arid savanna pollen record with the common savanna trees, grasses, local aquatic taxa combined with the deposition of well-dispersed montane taxa. Around 5000 cal year BP different sites across East Africa showed an increase in abundance of Poaceae at the expense of arboreal taxa in the lowlands, coupled with increases in montane forest taxa indicative of drier climatic conditions. The East African environment shifted towards a drier climate regime characterised by reduced precipitation, increased evaporation, and/or an extension or intensification of the dry season (Marchant and Hooghiemstra 2004). Isotopic data at Lake Malawi show an increase in C4 vegetation, initiated again around 4000 cal year BP, which is indicative of increasingly arid environmental conditions (Castañeda et al. 2009). A peak in aeolian dust around 4000 cal year BP also indicates regionally dry conditions resulting in increased dust deposition to the Kilimanjaro glacier (Thompson et al. 2002).
The Esambu record is characterised by a highly diverse mix of savanna and montane taxa, most likely a local signal of increased moisture in the mid to late Holocene (200–131 cm). A record from the Amboseli Basin at Namelok Swamp records a relatively moist environment about this time with the increased presence of Syzygium, a tree taxon that grows within waterlogged soils (Rucina et al. 2009) between 2150 and 800 cal year BP. After ~ 800 cal year BP, the record from Namelok Swamp indicates a drier environment with the increased presence of Amaranthaceae and Poaceae and decreased levels of Syzygium (Rucina et al. 2009). A dry climate, with increasing signals of human-ecosystem interaction, is observed from Lakes Naivasha and Challa (Westerberg et al. 2010; Buckles et al. 2015). Within the last c. 400 years (≤ 131 cm), the Esambu record was characterised by a decrease in abundance and diversity of woody taxa and an increase in the Cyperaceae-Poaceae ratio that could have resulted from increased human activity that impacted on the surrounding forests. The accompanying increase in charcoal abundance might have resulted from increased natural and anthropogenic ignition coupled with increased fuel connectivity and potentially lower grazing pressures.
Humans have been present within the landscape for many millennia: archaeological studies from Tsavo show evidence of domesticates from faunal diagnostic finds identifying the presence of cattle Bos taurus (Wright et al. 2007) from 3700 cal year BP. Despite this longevity of human presence, it is only fairly recently that human agency has become one of the key drivers of ecosystem composition and distribution. Pollen evidence for intensive human-induced land use modifications to local forest ecosystems extend back to c. 600 cal year BP at on Mount Shengena, northern Tanzania (Finch et al. 2016). Sustained and pervasive human impact, in the form of intensive crop cultivation across East Africa, occurs a little later, particularly over the last three to four centuries. Expanding forest clearance, particularly on the highlands of East Africa (Finch et al. 2016) and expansion of sedentary agriculture in the wider region is quite transformative on human-ecosystem interactions and tied into external drivers, particularly the expanding and increasing industrial ivory caravan routes and the arrival of New World crops. Zea mays can be detected within sedimentary records dates to 1810 AD on the Pare Mountains (Finch et al. 2016) and around 1650 AD at Lake Naivasha (Lamb et al. 2003). At Esambu, the presence of Poaceae pollen grains > 60 µm, which can be interpreted as being derived from cereal grasses, are accompanied by increased presence of macroscopic charcoal, and thought to be derived from more localised increased farming activity. Increased presence of Acacia, Amaranthaceae/Chenopodaceae, Balanites and Poaceae in the uppermost samples from Esambu, dating to the last 200 years, could be indicative of a drier environment, or a consequence of a decreased elephant population. Herbivores and elephants in particular, impart a major influence on vegetation composition, distribution and structure (Håkansson 2004; Guldemond and Van Aarde 2008). Although largely unquantified, the removal of millions of rhinoceros and elephants from the East African landscape via the ivory trade, that reached industrial proportions in the 18th and 19th centuries, would have been transformative on savanna and woodland composition and distribution.
Thus, there have been a range of ecosystem shifts within the Amboseli landscape that have increasingly moved from being driven by environmental variability towards anthropocentric factors, either via impact on elephant population, import of new crops or expansion of sedentary agriculture in replacement of nomadic pastoralism. These long-term insights into ecosystem human–environment interactions can be vital to inform adaptive management policies and defining boundary condition that such policies may want to achieve (Gillson and Marchant 2014). Such long-term insights are particularly important under current human-induced land use transformations and increasing impact of climate change and climate variability on the changing distribution of species (Platts et al. 2012). However, for these data to be able to inform such debates they have to be communicated to a range of stakeholders and the presentation of complex stratigraphic data (Figs. 4, 5) as a simple illustration (Fig. 6) is one potential way to make these data more accessible to a wider audience and can be incorporated into video media and made available on different platforms.
Although the palaeoecological study presented from Esambu swamp does not present a ‘pre-disturbance baseline’ to provide a management target, for example via for restoration ecology interventions to work towards some pristine natural state, it does provide an understanding of the local response of such wetlands to the regional drivers of change. Such understanding is crucial as these wetlands, and indeed the wider hydrological budget, is under increasing pressure through a combination of changing climates, population growth, sedentarisation and land use policies in a complex institutional landscape. Such insights can support the development of customised management plans that consider these interacting factors in operation across the landscape and clearly the influence of the different factors change through time. Viewing the Amboseli landscape as one that has been, and continues to be, transformed through centuries of human agency, provides temporal context for understanding the interactions that take place between the wildlife, livestock, people, and their ecosystems.
The pollen, NPP and charcoal in the Esambu sediment record provide a long-term record of ecosystem dynamics from the Amboseli, albeit with some chronological uncertainties. Sparse woodland and shrub taxa characterised the semi-arid Amboseli landscape from c. 5000 to sometime between 3500 and 500 cal year BP. Wetland expansion resulted in peat accumulation and preserved a high resolution record of vegetation variability in response to hydroclimatic variability and modifications by herbivores and, more recently, human land use changes. Current land cover and land use impacts over the past centuries years have resulted in the conversion of a portion of the wetland to agricultural production as human activity becomes much more visible within the Esambu wetland. Future studies in the region and at comparable wetlands in eastern Africa should focus on sedimentological analyses, relationships between sedimentology and geochronology, in addition to palaeovegetation.
The current Esambu swamp ecosystem has no analogue in the last c. 5000 cal year BP; this indicates the dynamic nature of the ecosystem as current conditions impact on the swamp leading to the emergence of a novel ecosystem reflecting modern day pressures. Understanding how ecosystems have evolved under these changing interactions of climate variability, human land use and land cover, wildlife use, and fire activity through time and across space is vital. This provides an informed context for future management choices that need to take into account that the system is shaped by numerous anthropogenic fingerprints through time.
We acknowledge Nicolas Deere for preparing MODIS fire products. We thank Carol Lang for preparing wood thin sections and taking optical light microscopy images and Delphine Joly and Robyn Veal for examining the wood fragment that was radiocarbon dated. Peter Omeny provided Kenya Meteorological Office Makindu weather data. We acknowledge the researchers who submitted data into the NOAA National Centers for Environmental Information and to all researchers who contributed East African data to the Global Charcoal Database. We thank Johnny Panga Brushworth for discussing his observations of environmental change in the region and Anna Shoemaker for facilitating a follow-up visit to the site in 2014. This paper is in memory of Dr. Ugo Zoppi who handled some of the radiocarbon dating. This research was partially funded by a European Commission Marie Skłodowska-Curie Initial Training Network grant titled ‘Resilience in East African Landscapes (REAL)’ (FP7-PEOPLE-2013-ITN project number 606879) to RM and supported ENG and CJCM. CJCM was also supported through the ‘Adaptation and Resilience to Climate Change (ARCC)’ project under the sustainability and resilience - tackling climate and environmental changes programme funded by Swedish Research Council (Vetenskapsrådet), Sida and Formas (2016-06355).
- Buckles, L.K., J.W.H. Weijers, D. Verschuren, C. Cocquyt, and J.S. Sinninghe Damsté. 2015. Short-term variability in the sedimentary BIT index of Lake Challa, East Africa over the past 2200 years: validating the precipitation proxy. Climate of the Past Discussions 11: 1177–1218.CrossRefGoogle Scholar
- Casanova, M.T., and I.J. Powling. 2014. What makes a swamp swampy? Water regime and the botany of endangered wetlands in western Victoria. Australian Journal of Botany 62: 469–480.Google Scholar
- Castañeda, I.S., J.P. Werne, T.C. Johnson, and T.R. Filley. 2009. Late Quaternary vegetation history of southeast Africa: The molecular isotopic record from Lake Malawi. Palaeogeography, Palaeoclimatology, Palaeoecology 275: 100–112. https://doi.org/10.1016/j.palaeo.2009.02.008.CrossRefGoogle Scholar
- Directorate of Overseas Surveys. 1963a. Amboseli sheet 181/1 [map]. Edition 2-SK. 1:50000. Survey of Kenya, Nairobi.Google Scholar
- Directorate of Overseas Surveys. 1963b. Kimana sheet 182/1 [map]. Edition 2-SK. 1:50000. Survey of Kenya, Nairobi.Google Scholar
- Fægri, K., and J. Iversen. 1989. Textbook of pollen analysis. New York: Wiley.Google Scholar
- Foley, R. 1981. Off‐site archaeology and human adaptation in Eastern Africa: An analysis of regional artefact density in the Amboseli, Southern Kenya. Cambridge Monographs in African Archaeology 3. BAR International Series 97.Google Scholar
- van Geel, B., V. Gelorini, A. Lyaruu, A. Aptroot, S. Rucina, R. Marchant, D. J. S. Sinninghe, and D. Verschuren. 2011. Diversity and ecology of tropical African fungal spores from a 25,000-year palaeoenvironmental record in southeastern Kenya. Review of Palaeobotany and Palynology 164. Elsevier B.V.: 174–190. https://doi.org/10.1016/j.revpalbo.2011.01.002.
- Guldemond, R., and R. Van Aarde. 2008. A meta-analysis of the impact of African elephants on savanna vegetation. Journal of Wildlife Management 72: 892–899.Google Scholar
- Kamau, P.N., and K.E. Medley. 2014. Anthropogenic fires and local livelihoods at Chyulu Hills, Kenya. Landscape and Urban Planning 124. Elsevier B.V.: 76–84. https://doi.org/10.1016/j.landurbplan.2014.01.010.
- Kenya Wildlife Service. 2008. Amboseli ecosystem management plan, 2008–2018. Nairobi, Kenya: KWS Protected Areas Planning Framework.Google Scholar
- Lane, P.J. 2013. The archaeology of pastoralism and stock-keeping in East Africa. In The oxford handbook of African archaeology, ed. P.J. Mitchell, and P.J. Lane, 585–602. Oxford: Oxford University Press.Google Scholar
- MEMR. 2012. Kenya Wetlands Atlas, 192. Nairobi, Kenya: Ministry of Environment and Natural Resources.Google Scholar
- R Development Core Team. 2015. R: A language and environment for statistical computing. Vienna, Austria: R Foundation for Statistical Computing.Google Scholar
- Reimer, P J., Hoper, S., McDonald, J., Reimer, R., Svyatko, S., Thompson, M., 2015. The Queen’s University, Belfast Laboratory Protocols used for the AMS Radiocarbon at the 14CHRONO Centre. Research Report Series 5-2015, English Heritage.Google Scholar
- Rourke, J.M.A., 2011. Seasonal prediction of African rainfall with a focus on Kenya (Doctoral dissertation, UCL (University College London)).Google Scholar
- Rucina, S. M., V. M. Muiruri, R. N. Kinyanjui, K. McGuiness, and R. Marchant. 2009. Late Quaternary vegetation and fire dynamics on Mount Kenya. Palaeogeography, Palaeoclimatology, Palaeoecology 283. Elsevier B.V.: 1–14. https://doi.org/10.1016/j.palaeo.2009.08.008.
- Sarkar, S. 2006. Long- and short-term dynamics of the Wetlands in the Amboseli Savanna Ecosystem, Kenya. PhD dissertation, University of Waterloo. http://hdl.handle.net/10012/2978.
- Westerberg, L.O., K. Holmgren, L. Börjeson, N.T. Håkansson, V. Laulumaa, M. Ryner, and H. Öberg. 2010. The development of the ancient irrigation system at Engaruka, northern Tanzania: Physical and societal factors. Geographical Journal 176: 304–318. https://doi.org/10.1111/j.1475-4959.2010.00370.x.CrossRefGoogle Scholar
- Wetlands International. 2009. Planting trees to eat fish: Field experiences in wetlands and poverty reduction. Wageningen, the Netherlands: Wetlands International.Google Scholar
- Williams, L.A.J. 1972. Geology of the Amboseli area (vol. 90). Geological Survey of Kenya, Ministry of Natural Resources, Republic of Kenya.Google Scholar
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