Relationship between vegetation and modern pollen-rain along an elevational gradient on Kilimanjaro, Tanzania

Modern pollen-rain studies are crucial for the calibration and interpretation of fossil pollen records. In East Africa, numerous pollen records provide important insights into the impact of human populations and climate change on tropical ecosystems. However, the confident use of fossil pollen data to reconstruct vegetation and climate dynamics requires well-founded knowledge regarding the relationship between pollen deposition and modern-day vegetation, which is still deficient for large parts of the African continent and non-existent for the tropical East African Mountains. In this study, we investigated the relationship between vegetation and modern pollen-rain along the elevational gradient of Kilimanjaro. We apply multivariate data analysis to assess the relationship between vegetation and modern pollen-rain and quantify the representativeness of forest zones. We further assessed the taxonomic level needed for differentiation between forest zones based on the modern pollen-rain assemblage, biodiversity patterns and pollen and spore drift. In the montane vegetation of Kilimanjaro, it is sufficient to analyse the pollen-rain on plant family level in order to derive the forest zone of the surrounding vegetation. Along this elevational gradient, pollen and spore dispersal is strongly influenced by regional wind patterns, but their deposition reflects the diversity patterns of the surrounding vegetation. This study represents the first statistical analysis of pollen vegetation relationship along an elevational gradient in Africa. Hence, this paper improves confidence in interpretation of palynological records from the tropical East African Mountains and may refine past climate reconstructions for a more accurate comparison of data and modelling.

Modern pollen calibration studies along latitudinal and longitudinal gradients in Africa demonstrate that pollen spectra within one particular vegetation zone are more similar to one another than these pollen spectra are to pollen samples from other vegetation zones (Gajewski et al., 2002); furthermore, a good latitudinal correspondence exists between the distribution patterns of pollen in marine surface sediments and the occurrence of the source plants on the adjacent continent (Dupont and Wyputta, 2003;Hooghiemstra et al., 2006).
Pollen-rain vegetation relationships along steep climatic gradients in the Neotropics show that pollen spectra closely reflect the vegetation composition of Amazonian montane forests (Urrego et al., 2011;Weng et al., 2004). The differentiation of pollen spectra from dry forest localities showed the potential of genus-level pollen data to reflect precipitation gradients. The authors also demonstrate that cloud and rainforest compositional changes along elevation gradients are well represented. Niemann et al. (2010) show that a high number of pollen and spore taxa are characteristic for one vegetation type, and that they reflect the altitudinal distribution of genera and families in the modern vegetation.
Additionally, in a modern pollen-rain elevational study from montane forests in western Amazonia, turnover along the elevational gradient provided a strong correlation with changing pollen spectra (Urrego et al., 2011). The authors demonstrate that longdistance pollen dispersal has little importance within the montane forest zone, and the downslope limit of forest taxa was reflected accurately in pollen spectra. However, Urrego et al. (2011) also show that transport of pollen to elevations above the tree line leads to significant over-representation of arboreal taxa in shrub and grassland environments.
The comparison between pollen-rain and plant distribution, which clarifies the relationship between plant assemblages and pollen deposition, is therefore essential for a more precise vegetation and climate reconstruction, as it identifies taxa that have high correspondence between pollen and plant distribution patterns. Several analyses of modern pollen-rain have yielded transfer functions relating pollen representation to environmental parameters as well as indicator taxa for particular ecosystems (Bush and Rivera, 2001;Gosling et al., 2009;Rodgers and Horn, 1996;Weng et al., 2004). However, the relationship between pollen assemblage and vegetation is not straightforward since differences in pollen production and dispersal cause some plant taxa to be over-represented in pollen records, while others are underrepresented (Jackson and Lyford, 1999;Prentice, 1985;Sugita, 1994;Tauber, 1967).
A major obstacle to progress in tropical palynology is the high diversity of species, and hence, pollen types. Despite this, much work has recently been done to improve the ability to identify fossil pollen from the tropics (Bush and Weng, 2007;Gosling et al., 2013), and much of the potential information in the record is still lost among the 'unknowns' (e.g. Marret et al., 2013). Furthermore, there is a general lack of understanding of the proportional representation of species (Bush and Rivera, 2001).
In the tropical forests of Barro Colorado Islands (Panama), Bush and Rivera (2001) found that wind-pollinated plants are generally over-represented, while animal-pollinated plants are underrepresented.
It is not clear to what degree the pollen assemblages represent local versus regional vegetation. A substantial proportion of pollen deposited in small basins (<30 m in diameter), or under a closed canopy, originates from vegetation growing close to the site (20-30 m), while pollen from a more distant source often overshadows the local signal in large basins >30-50 m in diameter (Jackson and Lyford, 1999;Jacobson and Bradshaw, 1981;Prentice, 1985;Sugita, 1993;Tauber, 1967).
Studies of closed canopy sites have shown a strong representation of pollen from non-local (>100 m) and even distant sources (>750 m), if non-local vegetation includes an abundance of taxa that produces large quantities of easily dispersed pollen (Calcote, 1995;Jackson and Kearsly, 1998;Jackson and Wong, 1994;Sugita, 1994). Upslope transport of pollen of wind-pollinated species (e.g. Alnus, Ulmus, Myrica and Quercus) is evident in the sparsely vegetated montane samples from Panama and Costa Rica (Bush, 2000). However, the corresponding downslope transport of these prolific pollen producers is masked by local pollen production.
In the Congo Basin, Elenga et al. (2000a) suggest that the pollen-rain and floristic composition of the vegetation are not linked to altitudinal or precipitation gradients but to hygromorphy and soil type. The results propose that only a few taxa (Symphonia globulifera, Uapaca, Hallea, Anthostema, Dialum and Sapotaceae) show a good correlation between plant cover and pollen abundance. Arboreal taxa dominate the pollen-rain, and the plant diversity is poorly reflected. The results by Elenga et al. (2000a) also propose that in dense lowland rainforest, most pollen grains only travel a distance of 20-50 m.
The studies of Lebamba et al. (2009) and Reese and Liu (2005), which focused on African (Cameroon, Gabon and Congo) and central Andean forests, highlight the potential of modern pollen data to accurately predict present-day vegetation in lowland and montane forest ecosystems.
Biomes reconstructed from modern pollen data (Prentice et al., 1996) accurately reflect the broad features in the vegetation map. For the tropical rainforest biome of South America, 85% of the sites accurately reflect the potential vegetation (Marchant et al., 2009).
In the montane forests of south-west Uganda, a close relationship was not always observed between the modern pollen-rain and present-day vegetation (Marchant and Taylor, 2000). The subsequent reinterpretation of the Holocene pollen record of the Mubwindi Swamp, SW Uganda, showed that the suggested dominance of Olea (Oleaceae) and Podocarpus (Podocarpaceae) around the swamp was erroneous (Marchant and Taylor, 1998;Marchant et al., 1997). Also, taxa such as Celtis (Cannabaceae), Ericaceae, Faurea (Proteaceae), Hagenia (Rosaceae), Macaranga (Euphorbiaceae), Nuxia (Stilbaceae), Olea (Oleaceae), Podocarpus (Podocarpaceae) and Schefflera (Araliaceae) were probably significantly less important components of the surrounding vegetation over the late Holocene than indicated by their pollen record.
In our study, we address the following questions: (1) how are the different plant taxa represented in the modern pollen-rain and why? (2) which taxonomic level is necessary to distinguish between the different forest zones observed in the vegetation (after Hemp, 2006a)? (3) are the biodiversity patterns of the modern vegetation reflected in the pollen-rain? and (4) what pollen drift effects do we observe by investigating and quantifying the modern pollen-rain-vegetation relationship along an elevational gradient on the southern slope of Kilimanjaro between 1900 and 3200 m a.s.l. (above sea level). Such a relationship between the vegetation composition and pollen-rain is essential for the calibration of available and future palaeo-records from Kilimanjaro (Schüler, 2013;Schüler et al., 2012) as well as in regions with similar vegetation composition. Multidimensional scaling (MDS) was used in early palynological studies to examine changes in pollen assemblages (Prentice, 1980). By comparing modern pollen and vegetation inventory data of plots at 100-m elevation intervals, we investigate the relationship between vegetation cover and pollen-rain. For the Neotropics, Punyasena (2008) shows that plant family level is sufficient for palaeo-environmental reconstruction across the range of several different tropical regions. Since this so far has not been shown for smaller scale ecosystems and the identification of tropical pollen grains to a generic or species level remains difficult (e.g. Elenga et al., 2000a), we apply non-metric multidimensional scaling (NMDS) to detect the adequate taxonomic level of pollen grain identification for reliable results on the corresponding afromontane vegetation. By comparing plant and pollen abundances, we assess biodiversity patterns as well as pollen and spore dispersal along the elevational gradient of Kilimanjaro.
Despite numerous studies on regional palaeoecology, few studies have characterized the palynological signatures of tropical montane ecosystems, hindering efforts to make ecological inference from palynological data. Despite its small sample size, the data set presented here represents the first statistical analysis of the pollen vegetation relationship along an elevational gradient in Africa, improving the interpretation of palynological records from the tropical East African mountains.

Study area
Kilimanjaro (Figure 1a) is located 300 km south of the equator in Tanzania on the border with Kenya between 2°45′ and 3°25′ south and 37°00′ and 37°43′ east. Kilimanjaro is an eroded relict of an ancient volcano with three peaks (Shira, Mawenzi and Kibo) rising from the savannah plains at 700 m elevation to a snow-and ice-clad summit of 5895 m a.s.l. (Downie et al., 1956) ( Figure 1b). Kilimanjaro has a diameter from north-west to south-east of 90 km.
The investigated vegetation gradient extends from 1900 m a.s.l. in the submontane forest to the upper forest border at 3200 m a.s.l., and is located in close proximity to the river Weru-Weru ( Figure 3c).

Climate
According to Köppen and Troll/Pfaffen (Müller, 1989) the Kilimanjaro area is characterized by a seasonally dry, tropical climate. Because of the influence of the position of the ITCZ and its proximity to the equator, Mt Kilimanjaro is characterized by a bimodal rainfall pattern and experiences four hydrological seasons per year: one short dry season in January and February, a long rainy season from March to May, a long dry season from June to September followed by a short rainy season in November and December.
The climate on Mt Kilimanjaro is further dependent on the elevation on the mountain and the exposition of the mountain side. Because of the prevalence of SE trade winds, the southern slope is generally wetter than the northern slope. Mean annual precipitation at the lowest pollen plot at 1950 m a.s.l. is about 2670 mm/yr and increases to over 3050 mm/yr between 2050 and 2350 m a.s.l. At higher elevations, precipitation decreases to <1480 mm/yr above 3250 m a.s.l. The mean annual temperature decreases from 14.3°C at 1950 m to 7.1°C at 3250 m a.s.l. with a lapse rate of 0.6°C. Frost starts at 2950 m during cool nights in July and August (Hemp, 2006a). The predominance of the southeasterly trade wind at Kilimanjaro is modified by the mountain's topography causing strong downhill winds during the evening hours and weaker uphill winds during daytime (Hemp and Zimmermann, unpublished).

Vegetation
Covering about 5000 km 2 , Kilimanjaro has several distinct bioclimatic zones ( Figure 1b) (Hemp, 2006a): A dry and hot colline savannah zone surrounds the mountain base between 700 and 1100 m a.s.l. Most of this area is used for crop production or as pastureland. Remnants of the former savannah vegetation with Acacia (Mimosaceae), Terminalia (Combretaceae), Grewia (Malvaceae) and Combretum (Combretaceae) woodlands are present mainly around Lake Chala in the eastern foothills and on the north-western side of the mountain. The submontane and lower montane forest (LMF) belt between 1000 and 1800 m a.s.l. have been converted to coffee-banana fields in the 'Chagga homegardens', a type of traditional agroforestry. Remnants of the former forests of this zone with Newtonia (Mimosaceae), Strombosia (Olacaceae) and Entandrophragma (Meliaceae) rarely occur outside of deep valleys and gorges.
The pollen trap transect ( Figure 1c) starts in the LMF zone (defined after Hemp, 2006a), where Macaranga kilimandscharica (Euphorbiaceae), Agauria salicifolia (Ericaceae) and Ocotea usambarensis (Lauraceae) are the dominant tree species. This part of the transect is influenced by human activities such as fodder and wood collection and grazing by cattle.
Most vegetation study plots are located in the middle-montane forest (MMF) zone, which starts in the Weru-Weru area at 2200 m a.s.l. In this zone, humidity reaches its maximum value, indicated by the wealth of epiphytes and ferns, in particular filmy ferns and tree ferns. O. sambarensis (Lauraceae), Xymalos monospora (Monimiaceae), Ilex mitis (Aquifoliaceae) and Schefflera volkensii (Araliaceae) comprise the tree layer.
In the upper montane forest (UMF) zone above 2800 m a.s.l., Podocarpus latifolius (Podocarpaceae), Hagenia abyssinica (Rosaceae) and Prunus africana (Rosaceae) form the tree canopy. Additionally, monodominant stands of Erica excelsa (Ericaceae) play an important role in this zone, replacing Podocarpus and H. abyssinica forests after fire, forming the upper closed forest line on the southern slope of Kilimanjaro at 3250 m a.s.l. Above 3250 m a.s.l., the cloud forests are replaced by Erica heathlands. Erica trimera forest remnants at 4000 m a.s.l. indicate the upper potential natural forest line. Above this altitude, the Erica heathlands change into Helichrysum (Asteraceae) dwarf cushion vegetation that extends up to 4500 m a.s.l. The highest altitudinal region is very sparsely vegetated and the top of Kibo, the main summit, is covered with glaciers. For a more detailed description of these vegetation types, see Hemp (2001Hemp ( , 2006aHemp ( , 2006c.

Floristic inventories
On the Weru-Weru transect, research plots at 100 m altitudinal intervals with vegetation records, soil profiles, rain gauges and data loggers for temperature and humidity were established in 2005. For our study, we used the 15 plots between 1950 and 3250 m a.s.l., since the forest below 1900 m a.s.l. is heavily disturbed and frequented by people collecting firewood and fodder. The plots measured 50 m × 50 m. The plot size was chosen with respect to the minimum area calculated with the nested plot method (as suggested by Mueller-Dombois and Ellenberg, 1974). Three plots were located within the LMF (1900-2100 m a.s.l.), eight in the MMF (2200-2800 m a.s.l., including one additional plot at the upper distribution border of Cyathea manniana) and four in the UMF (2900-3200 m a.s.l.). Plant taxa abundances were estimated using the Braun-Blanquet (1964) cover-abundance scale for vegetation analysis. Estimating the coverage and abundance of plant species is one of the methods of vegetation description.

Modern pollen-rain sampling and laboratory methods
In total, 30 pollen traps were installed along the elevational transect used for the floristic inventories (see above) in February 2010. Two traps were installed at every vegetation plot. The same pollen trap type was used as suggested by Behling et al. (2001) and Niemann et al. (2010) using 50-mL test tubes with 3 mL glycerine and synthetic cotton and a net as cover installed 10 cm above the ground. In all, 26 pollen traps were recollected in February 2011 (Table 1).
Pollen was extracted from the 'Behling traps' by centrifuging and sieving the samples. Afterwards, acetolysis was carried out on the samples to dissolve cellulose material and to stain the pollen residues. The pollen residue obtained was kept in distilled water until mounted into glycerol jelly for pollen analysis. For each sample, we counted at least 300 pollen grains. Fern spores were also counted and expressed as percentages of the pollen sum (but not included in it). Pollen and spore identification was based on the reference collection of about 2000 slides of the Department of Palynology and Climate Dynamics, Göttingen University, the African Pollen Database (Lézine, 2001) and relevant literature (Bonnefille, 1971).
A pollen percentage diagram was compiled with the software C2 Version 1.7.2 (Juggins, 2011), illustrating the most abundant and ecologically important taxa ( Figure 3). Pollen taxa were assigned to forest zones in accordance with Hemp (2006a).

Multivariate data analysis
NMDS was applied to investigate the similarity between pollen traps within one plot, the representivity of the surrounding vegetation by pollen-rain composition and the taxa level needed to be able to differentiate between forest zones based on the modern pollen-rain assemblage.
NMDS is a data reduction technique that projects multivariate data along latent axes in distance measure-based space and preserves the underlying dissimilarity structure between points (McCune et al., 2002). In this way, highly multivariate data can be represented in a lower dimensional space while preserving the data structure. In contrast to 'conventional' ordination methods such as canonical correlation analysis, NMDS effectively combines the shared variance of implicit causal factors along the axes rather than defining the structural attributes a priori (McCune et al., 2002).
The NMDS was performed using the meta-MDS function contained in the vegan package for R (Oksanen et al., 2013). Pollen proportions were calculated based on the total of the pollen subset selected for analysis: 126 identified pollen types. The species data were square root transformed as suggested for community data with skewed abundance distribution and many zero values. The NMDS distance matrix was calculated using the Bray-Curtis distance between study sites based on the square-root-transformed pollen data. Constrained ordination procedures were not used because long-distance pollen transport and narrow elevation (and thus temperature and precipitation) gradients are likely to result in violations of the underlying assumptions of these methods. Among unconstrained ordination procedures, principal component analysis is a poor choice as it assumes linear relationships between variables and short ecological gradients (Kent, 2006), requiring multivariate normality (McCune et al., 2002). The pollen and climate data in this study do not meet these assumptions, which limits our ability to apply the technique of Anderson and Willis (2003) who recognize that canonical analysis of principal coordinates cannot replace NMDS for certain applications. Because NMDS evaluates data structure using dissimilarity measures, it allows estimates to be made based on dissimilarity and directionality. Furthermore, as points are placed into space using information from the entire data set rather than one or several proximate points, problems associated with spatial autocorrelation (Telford and Birks, 2005) are mitigated. The dimensionality of the final ordination was determined when the Kruskal stress of the ordination declined successively by increasing dimensions (McCune et al., 2002). The maximum number of random starts in search of stable solution was set to 100. For the investigation of the influence of the taxonomic level on the possibility to derive certain forest zones from the pollenrain, the pollen types were assigned to their plant families (67 identified families in total).

Representativeness of plant families in the modern pollen-rain
Some pollen types are difficult to determine at genus level but can easily be assigned to a plant family. Hence, for the data analysis, the identified pollen types were pooled on family level. To investigate how the vegetation is represented in the pollen traps, we compare the percentages of plant families present in the vegetation cover and in the pollen-rain. This was done separately for every forest zone (LMF, MMF and UMF) for all plant families present in both data sets. To enable calibration according to the relationship between the percentage of the family within the pollen trap and the surrounding vegetation, we generate a transfer factor (TF = (% taxon in vegetation)/(% taxon in pollen-rain)). This factor, which can also be applied to fossil pollen data (Marchant and Taylor, 2000), compensates for differences in representativeness of pollen. The comparison of the transfer factors of the different forest zones also allows further ecological conclusions on pollen production and dispersal.

Assessing biodiversity
Plant diversity was assessed by comparing the number of plant families in the pollen traps and in the corresponding vegetation plot. This comparison was also done on generic and specific level of plant taxa and pollen types.

Pollen and spore dispersal
For assessing pollen and spore dispersal, we made a comparison between the abundance of Cyperaceae and Cyathea in the vegetation and in the modern pollen-rain. Those two taxa are very abundant and most likely to capture the wind pattern in their pollen/ spore distribution. Cyperaceae release their pollen during day and night, while the sporangia of Cyathea are only open only during the day when climate conditions are dry. Both taxa have defined ecological limits of their distribution within the studied altitudinal transect which facilitates the detection of pollen/spore shifts. In each case, the vegetation cover and the pollen/spore data were plotted against the altitude. For the vegetation cover, we applied a moving average to the data set (window size of 3) to smooth out short-term fluctuations caused by the transformation of the Braun-Blanquet (1964) scale into percentage values, and to highlight long-term trends.

Multivariate data analysis
The NMDS of the modern pollen-rain data (Figure 2) provides information on the differences between individual pollen traps and between different vegetation plots derived from the modern pollen-rain data based on identified pollen types and at family level. The degree of correspondence between the distances among points implied by NMDS diagram, and the data matrix input is measured (inversely) by a stress function called Kruskal stress. When the NMDS diagram perfectly reproduces the input data, the stress value is zero. For all three ordinations, the Kruskal stress was reduced to values below 0.1 when using three dimensions in the NMDS.
In Figure 2a, the NMDS of the individual pollen traps based on the pollen types is shown (Kruskal stress: 0.085). Pollen traps of the same plot are clustered. Furthermore, samples of the pollen traps ranging from 1900 to 2100 m a.s.l., which correspond to the LMF (Hemp, 2006a), are grouped as well as samples from 2200 to 2400 m a.s.l. (lower mid-montane forest, lMMF), 2500 to 2800 m a.s.l. (upper mid-montane forest, uMMF) and 2900 to 3200 m a.s.l. (UMF).
In Figure 2b, the NMDS of the pollen traps -pooled per plot -based on the pollen type families is shown (Kruskal stress: 0.048). The pattern of the sample distribution is similar to the one revealed by the NMDS based on the pollen types (Figure 2a

Representativeness
The pollen percentage diagram (Figure 3) of modern pollen-rain shows sums of forest zones, LMF, MMF and UMF, and most  , and selected pollen taxa grouped into these forest zones. The two respective pollen data sets per plot were merged. Grouping of taxa is based on (Hemp, 2006a). The diagram shows that it is possible to distinguish between forest zones based on the pollen-rain assemblage.

Biodiversity
The plant diversity shows a decreasing trend with increasing elevation in the vegetation. This is also found in the modern pollenrain ( Figure 5). In the vegetation, the highest number of species (85) and families (51) is recorded at 1900 m a.s.l. The number of species reaches another maximum at 2700 m a.s.l. (69 species) and then decreases to 31 species in 23 families at 3200 m a.s.l. The diversity found in the modern pollen-rain has its minimum at 2000 m a.s.l., with only 19 pollen types in 16 plant families, it reaches 81 pollen types in 40 families at 2200 m a.s.l. and then decreases again to 29 pollen types in 23 plant families at 3200 m a.s.l. The pollen diversity is generally lower than the diversity in the vegetation, but they approximate with increasing elevation. At 2200 m and at 3100 m a.s.l., the number of plant families recorded in the modern pollen-rain exceeds slightly the number of families in the vegetation.  Cyperaceae in the surrounding vegetation cover (Figure 6b) shows different distribution patterns. Cyperaceae contribute between 0.5% and 3% of the total modern pollen-rain up to an elevation of 2400 m a.s.l. At 2600 m a.s.l., they reach a maximum of 4%, followed by a strong decrease of Cyperaceae pollen to less than 2% at higher elevations. In the present-day vegetation, Cyperaceae are most abundant (38% vegetation cover) around 2800 m a.s.l. Between 2300 m and 2700 m a.s.l., the abundance fluctuates between 5% and 16%. At lower elevations, Cyperaceae only represent 1-2% of the vegetation.

Interpretation and discussion
The NMDS of the individual pollen traps (Figure 2a) reveals only minor differences of modern pollen-rain assemblages between the pollen traps within one plot. Consequently, the individual pollen traps are similarly representative of the surrounding vegetation.
Some differences between the pollen traps, for example, at 3100 m a.s.l., are caused by the abundance of H. abyssinica. H. abyssinica is a strong pollen producer, but because of the relatively large pollen grains, the pollen dispersal over larger distances is rather low (Jackson and Lyford, 1999). Hence, the dominance of H. abyssinica pollen in the modern pollen-rain is likely to be a local signal because of the presence of single H. abyssinica trees. The close similarity of taxa composition within pollen traps of one plot is an essential prerequisite for any further investigations.
The NMDS also shows that the pollen traps are not only representative for the vegetation of the direct surroundings but also for the corresponding vegetation zone described by Hemp (2006a) along the elevational gradient of Kilimanjaro (see also Figure 3). The resemblance of samples of the same forest zone (LMF, MMF and UMF) is much higher than in-between the forest zones.
In the LMF, M. kilimandscharica (Euphorbiaceae), a wind-pollinated species, is very abundant in the vegetation and the major component of the pollen-rain record. The over-representation of M. kilimandscharica in the LMF is also likely because of the species' ability to produce vast amount of pollen grains.
Abundant Cyperaceae, Rubiaceae, Moraceae, Urticaceae, Piperaceae, Araliaceae, Podocarpus and Ilex generally characterize the vegetation of the MMF. However, two forest subtypes, as described by Hemp (2006a), can be detected in the modern pollen-rain: the lower MMF (2200-2400 m a.s.l.) and the upper MMF (2500-2800 m a.s.l.). The lower MMF (2200-2400 m a.s.l.) is characterized by abundant Schefflera (Araliaceae), Begonia (Begoniaceae), Ilex (Aquifoliaceae) and several Rubiaceae taxa (Psychotria, Pavetta, Pauridiantha). The relative strong abundance of Podocarpus and Urticaceae (Pilea) in the pollenrain represents the vegetation cover of the upper MMF (2500-2800 m a.s.l.). Podocarpus is most abundant at 2700-2800 m a.s.l., which is also reflected in the modern pollen-rain. In addition, Prunus and Rubus (both Rosaceae) can be used as indicator taxa for this upper MMF in the pollen record.
The UMF above 2900 m a.s.l. is dominated by H. abyssinica (Rosaceae) and Erica (Ericaceae) as a result of forest fires during the past. The abundance of Hypericum (Hypericaceae), Valeriana (Valerianaceae) and Violaceae in the pollen-rain also indicates a more open forest structure. Artemisia (Asteraceae), Geranium (Geraniaceae), Protea (Proteaceae) and Myrsine (Myrsinaceae) are typical taxa of the Erica zone, which replaces the UMF above 3200 m a.s.l.
The forest zones observed in the present-day vegetation are reflected well in the modern pollen-rain composition, independent on which taxonomic level is analysed. More specifically, our results indicate that the modern pollen-rain composition using only plant families is already very decisive when aiming at distinguishing between LMF, lower and upper MMF and UMF along the elevational gradient. Therefore, our results support the suggestion by Minckley and Whitlock (2000) that it is not always necessary to use the full suite of pollen taxa present if the goal is to reconstruct vegetation at the level of vegetation type or zone.
Even though the dominant plant families in the pollen-rain are not in all cases also the abundant ones in the vegetation, their occurrence facilitates the detection of forest zones, as is also suggested by Niemann et al. (2010). The more detailed ecological interpretation and floristic characterization within the forest zones can then be continued based on key taxa. Nevertheless, some aspects have to be taken into account. First, plant families consist in most cases of many species, which can have different ecological demands. Second, the pollen productivity and dispersal vary between species. As many tropical trees are animal pollinated (Bawa and Hadley, 1990), the relationship between pollen deposition and plant distribution is not linear. The representativeness of a plant family adds important qualitative information for the interpretation. Our results show that the representativeness of a plant family is not the same in all the forest zones (each spanning an elevational difference of 300-500 m). However, Ericaceae and Euphorbiaceae (mainly Macaranga) are strongly over-represented in the pollen record of the forest zones. Both Ericaceae and the genus Macaranga are strong pollen producers and have comparably small pollen grains, which would lead to such a representativeness pattern. Their pollen grains also seem to be subject to long-distance dispersal since they are recorded in plots where they do not appear in the vegetation.
Taxa that have a high TF value and that occur as silent taxa (present in the flora but unrecorded in pollen-rain) such as Hypericaceae or Balsaminaceae indicate weak pollen production and insect pollination. Taxa which appear with a low TF in one forest zone and are not in vegetation but in pollen record ('x' in Table 2) in other zones suggest that they are strong pollen producers (e.g. Erica) or their pollen is wind transported (e.g. Myrica).
The over-representativeness of Ericaceae, Rosaceae (H. abyssinica), Euphorbiaceae (M. kilimandscharica), Podocarpus and Araliaceae supports the finding of Marchant and Taylor (2000) who show that these taxa are probably significantly less important components of the surrounding vegetation than indicated by the modern pollen-rain.
The elevational gradient of plant diversity shows a humpshaped elevational species richness pattern which is known from other elevational gradient studies on mountain systems, and it is assumed to be related to the overlap of distributional ranges and the absence of extreme life conditions (Becker et al., 2007). This range-overlap effect is known to be particularly pronounced in the transition zone from montane forests to alpine vegetation (Kessler, 2001;Körner, 2003). On Kilimanjaro, this was shown for overall vascular plant diversity and in particular for Pteridophytes in relation to habitat variety, which is a major controlling factor of species richness (Hemp, 2002). At the upper forest border, fires start to become important on Kilimanjaro, creating a mosaic of different fire-induced successional stages of forest, shrub and tussock grassland stands (Hemp and Beck, 2001). Here, high community (beta) diversity in the fire-influenced areas of the upper montane zone leads to a higher species (alpha) diversity as compared with the closed undisturbed forest at lower altitudes and the monotonous Erica bush at higher altitudes (Hemp, 2001(Hemp, , 2006b.
We observe a similar overlap effect in the pollen diversity pattern. Highest values for pollen diversity are found in forest-type transition zones where the taxa composition in the vegetation changes substantially. This is the case at 2100-2200 m a.s.l., the transition from LMF to MMF, and at 3100-3200 m a.s.l. where the montane forest is replaced by ericaceous and alpine vegetation.
The diversity trend captured in the modern pollen-rain reflects the plant diversity in the vegetation. Substantial differences in numbers of taxa are probably because of the high proportion of insect-pollinated plants in the tropics (Bawa, 1983), which are mostly not or only rarely recorded in the pollen-rain. Towards more open vegetation in the UMF and the Erica zone, the pollen diversity reflects the plant diversity much better. It seems that our results in tropical montane vegetation confirm the finding by Tauber (1967) who proposed that under closed canopy cover, the pollen assemblage is a more local signal, whereas in more open areas, a wider range is recorded. Consequently, the pollen diversity reflects the plant diversity pattern independent of the investigated taxa level but that it can only be interpreted in consideration of the specific vegetation type and surrounding flora. Unlike the findings by Elenga et al. (2000a), our results from Kilimanjaro propose a good reflection of diversity patterns in the modern pollen-rain.
Cyperaceae recorded in the pollen-rain is only to some extent correlated to the present-day vegetation distribution of Cyperaceae. The results suggest a downwards shift of the distribution pattern reflected in the pollen-rain. The maxima of the Cyperaceae abundance in the vegetation at 2800 m and between 2400 and 2600 m a.s.l. are recorded about 500-600 m lower in the pollen-rain. Cyperaceae, which are wind pollinated, have rather light and non-sticky pollen so that they can be transported by air currents. Hence, this downslope shift of Cyperaceae pollen signal is likely caused by strong downward winds, which prevail on the slopes of Kilimanjaro during evening time. In contrast, the spores of Cyathea are large (between 80 and 120 µm) and not easily transported over long distances. The spore record of Cyathea reflects an average shift by only about 200 m elevation; however, in an upward direction. While the highest occurrence in the vegetation is at 2850 m a.s.l., Cyathea spores can still be found in the pollen traps at 3200 m a.s.l. This could be explained by the characteristic of ferns to release their spores under dry environmental conditions, which prevail during daytime, which is also the time of upward winds along the slopes of Kilimanjaro. Hence, our results suggest a positive correlation not only between the pollen/ spore drift and wind direction but also between drift distance and the wind force.
Our results show that even in closed canopy sites, there is a representation of non-local (>100 m) sources. This agrees with the findings by Sugita (1993) and Jackson and Wong (1994). However, our results show that in closed canopy sites, non-local taxa with low pollen production are also represented.
In the forests of Panama and Costa Rica, wind-dependent pollen transport was also observed for sparsely vegetated montane zones (Bush, 2000). In contrast to these findings, we do not observe a masking effect by local vegetation in the downslope transport into more dense vegetation.

Conclusion
Our modern pollen-rain study along the elevational gradient on Kilimanjaro reveals that it is crucial to establish a modern pollenrain -vegetation relationship for the calibration and interpretation of a fossil pollen record from mountain sites. It is possible to analyse the pollen-rain on plant family level in order to derive the forest zone of the surrounding vegetation and with this assess the climatic conditions, which is important for the interpretation of palaeo-records. The occurrence of plant families along the altitudinal gradient is differently represented in the modern pollen depending on various reproduction factors. This can be quantified as a transfer factor, which will be applied to calibrate palaeopollen data in future studies. The diversity trend captured in the modern pollen-rain reflects the plant diversity in the vegetation, but we observed differences in the taxa richness. The pollen and spore dispersal seems to be strongly influenced by the regional wind patterns. This needs to be considered when deriving past distribution ranges from pollen records.
Our results facilitate the confident use of fossil pollen data to reconstruct, more precisely, potential vegetation and its dynamics in East African montane forests, and to refine climate reconstructions based on transfer functions.