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1 November 2014 A Broad Transition from Cloud Forest to Páramo Characterizes an Undisturbed Treeline in Parque Nacional Llanganates, Ecuador
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This study aimed at investigating the vegetation pattern associated with the transition from upper northern Andean cloud forest to páramo grassland in a relatively unmodified area in Ecuador's Eastern Cordillera. Single 20 × 10 m plots were randomly placed in representative sites along an altitudinal gradient from continuously wet Andean montane cloud forest at 3400–3700 m to páramo grassland at 3900–4000 m. Also sampled was a disjunct stand of the stem-rosette Espeletia pycnophylla var. llanganatensis, some 200 km south of the limit of the otherwise continuous distribution of this genus. Several physical and chemical soil factors, including temperature at -30 cm, were determined. Visual estimates of cover in four life-form classes (trees, shrubs, herbs, ground cover) at each site revealed similarities related to their relative proximity along an elevation gradient. Stands with a tree cover were more species-rich than those without, due largely to the differential distribution of the woody flora. No abrupt discontinuity occurred in the mix of species along this gradient. Soil temperature and altitude were the most important factors of those measured to explain the variability in plant community structure and composition. There was no clear zonation evident along the altitudinal gradient, with vegetation structure and floristics displaying continuous variation. No clear upper forest limit was differentiated. The isolated presence of Espeletia in the area is discussed, but the theory about its origin remains speculative.


The highest parts of the wet perhumid northern tropical Andes consist of fragile landscapes characterized by a high biodiversity (Körner and Spehn, 2002; Price, 2006). These ecosystems include alpine páramo grasslands and humid montane cloud forests, which originally covered large tracts in Venezuela, Colombia, Ecuador, and Peru (Luteyn, 1999; Hofstede et al., 2003). Inhabitants of these regions reflect complex cultural and socio-economic circumstances. Most communities are made up of indigenous peoples and mestizo farmers that rely almost entirely on subsistence use of the natural resources, principally for agricultural production (Ange Jaramillo et al., 2002; Hofstede, 2011; Cuesta et al., 2012). Additionally, these landscapes provide important ecosystem services, particularly potable water for drinking and irrigation (Buytaert et al., 2006; Buytaert and de Bièvre, 2012), as well as carbon storage (Farley et al., 2005; Cabaneiro et al., 2008; Chimner and Karberg, 2008).

Over recent decades, population pressure on the ecosystems of the tropical high Andes has rapidly increased and agricultural land use has greatly expanded, often using inappropriate techniques and leading to serious land degradation (Podwojewski et al., 2002; López Sandoval, 2004). Natural montane cloud forests have been widely replaced by either potato cultivation, pastures for dairy cattle, or exotic conifer forest plantations, with native p´ramo grasslands being over-exploited by grazing combined with frequent burning (Hofstede, 1995; Verweij, 1995; Hofstede et al., 2002; Farley et al., 2004; González et al., 2011). In many situations, these developments have led to a depression of the upper forest limit (Laegaard, 1992; Sarmiento, 2002; Wille et al., 2002). If the uppermost forest is destroyed by human activities, páramo grassland from above the natural forest limit tends to colonize the cleared areas and thus over time can extend to lower altitudes than would otherwise be the case. By contrast, the upward movement of forest, attributed to the effects of contemporary global warming, has also been reported (Innes, 1991; Grabherr et al., 2010; Kessler et al., 2011; Jantz and Behling, 2012). These two factors, when combined, have potentially opposing effects, leading to complications when formulating predictive scenarios (Castaño, 2002; Grace et al., 2002; Tonneijck et al., 2006; Bader et al., 2007).

What limits tree growth at alpine treelines has been explained in various ways, mostly with low and variable daily temperatures as principal factors, with precipitation and wind stress as additional considerations (Acosta Solis, 1984; Körner, 1998, 2012), locally or regionally. However, the exact position and structure of the treeline may be determined by low average and extreme temperatures as well as other microclimatic factors, such as strong irradiance (Wardle, 1971; Miehe and Miehe, 1994; Germino and Smith. 1999; Körner and Paulsen, 2004; Körner, 2012), along with the ecology of the particular species involved (Smith, 1994; Bader, 2007; Llambí et al., 2013). The páramo itself is a tall tussock grass—dominated treeless tropical-alpine vegetation belt that extends from approximately 3400 m to over 4500 m altitude. Often a shrub-dominated (subpáramo) transition from upland forest to páramo is recognized, spanning an altitudinal range of ∼300 m (Salamanca, 1992), but from ∼3600 m to 4100 m, the vegetation is dominated by tussock grasslands (grass páramo). Above these altitudes from ∼4100 m to 4800 m, a more open, shorter cover occurs, the so-called superpáramo vegetation (Cuatrecasas, 1958; Cleef, 1981; Sklenár and Balslev, 2004).

There is a distinction between the limit of closed forest and that of tree growth; the two are not necessarily the same (Körner and Paulsen, 2004; Körner, 2012). Thus, although the páramo belt is essentially a treeless vegetation, patches of high-Andean dwarf forest and shrubland, up to 10 m tall, may occupy more sheltered sites between 3400 and 4300 m elevation (Ulloa Ulloa and Jørgensen, 1993; Young and Keating, 2001; Ramírez et al., 2009; Contreras, 2010; Llambí et al., 2013). The significance of these patches of dwarf forest above the present upper forest limit is debated (Wille et al., 2002). According to some authors (Cuatrecasas, 1958; Ellenberg, 1958, 1979; Laegaard, 1992; Sarmiento, 2002), these fragments are remnants of previous extensive forests destroyed by people. Further, by this reasoning, the uppermost limit of closed forest has been estimated to be as high as 4100 m in the Ecuadorian Eastern Cordillera, and 4350 m in the Western Cordillera (Laegaard, 1992), and is relatively abrupt. However, other studies have proposed natural causes for the occurrence of at least some forest fragments and individual trees that occur above the present-day continuous forest limit (Wille et al., 2002; Bader, 2007; Ramírez et al., 2009), thus by implication inferring a more gradual transition from closed forest to grassland. The occurrence of these forest patches has been variously explained: in relation to such factors as locally favorable microenvironmental conditions (Walter and Medina, 1969; Smith, 1978; Lauer, 1981; Bader et al., 2007), and/or specific physiological adaptations or complex species-specific local spatial interactions that allow certain tree species at relatively high altitude to establish and compete in the tall grass matrix (Vélez et al., 1998; Llambí et al., 2013).

The present vegetation pattern in the tropical high Andes is generally determined by human impact, particularly through the use of fire, leading to the destruction of woody vegetation usually on all but the most sheltered sites (Hofstede, 1995; Verweij, 1995; Hofstede et al., 2002; Young, 2009; Cuesta et al., 2012). Thus, few examples of what could be construed as a natural upper forest boundary now exist. Further, with the differing interpretations of past forest extent and altitudinal vegetation patterns, the degree to which human activity is the overriding cause of an apparently low upper forest limit and the present situation of widespread páramo, remains unclear (Bader et al., 2007; Young and León, 2007). The nature of the upper forest limit and the associated distribution of woody vegetation where there has been negligible human activity is thus open to question, and there is a clear need to identify reference sites (Bader et al., 2007; Ramírez et al., 2009). Such sites by implication, inevitably would be in remote locations with difficult access, thus presenting considerable logistical and practical problems for research. These factors have no doubt contributed to the current lack of knowledge of natural altitudinal vegetation patterns in the tropical high Andes (Miehe and Miehe, 2000). Notwithstanding these constraints, we aimed to identify a suitable location where, in the apparent absence of human activity, a natural altitudinal vegetation pattern covering a forest to páramo transition could be described and quantified both structurally and floristically. As such, we aimed to provide much-needed reference data enabling us to contribute to the debate on upper forest limits in the tropical high Andes.

Our criteria were met in the heart of Parque Nacional Llanganates, in the Ecuadorian central Eastern Cordillera, which includes one of the least disturbed areas of forest and páramo remaining in the northern Andes. Covering 2197 km2, the park has an altitudinal range from 1200 m on the Andean footslopes to the east (Amazon side), up to 4638 m at its highest point (Cerro Hermoso), near the western boundary (Fig. 1). Road access to, and agricultural use of, the páramo occurs only in the northern portion of the park, more than 30 km from the study site. The rest is without human use; indeed, few people enter and there is no discernible evidence of fire or domestic animals. Although there are indications of some pre-Hispanic use of certain peripheral parts (Anhalzer, 1998), it is highly unlikely that human impact, including fire, has determined any significant aspect of the present landscape. Importantly, Parque Nacional Llanganates is also home to a single stand of the emblematic páramo endemic stem-rosette of the genus Espeletia, located in a remote part of the park. This population is some 200 km south of the limit of continuous distribution of this taxon from Venezuela to northern Ecuador (Monasterio and Sarmiento, 1991; Cuatrecasas, 2013). This biogeographical anomaly is still awaiting a satisfactory explanation. Being situated just below the forest-páramo ecotone, it is a prominent feature in our study area, and we will also discuss potential mechanisms explaining its presence here.

Study Area

Parque Nacional Llanganates occupies the Llanganates Cordillera, which is dominated by Paleozoic metamorphic outcrops consisting of gneiss and quartzite (Llanganates Group). As such, the geology of the park contrasts with that of the surrounding areas. Though this formation constitutes the basis of the major part of the Ecuadorian Eastern Cordillera, elsewhere these rocks have been covered by volcanic formations of Tertiary and Quaternary age (Jørgensen and Ulloa Ulloa, 1994; Vázquez et al., 2000). Also, the higher parts of the Llanganates Cordillera have been heavily eroded by glacial activity during the Pleistocene, resulting in a rolling landscape with U-shaped valleys, many glacial lakes and mires, along with rocky outcrops in cirques and lateral moraines. Furthermore, it is likely that the metamorphic rocks are less permeable than those of volcanic origin, leading to more ponds and lagoons on the valley floors in the Llanganates Cordillera when compared with other parts of the Eastern Cordillera. Soils in the region are influenced by volcanic ash deposits from neighboring active volcanoes, such as Cotopaxi and Tungurahua, that have covered the entire Llanganates Cordillera (Mothes, 1991 ; Vázquez et al., 2000).

The park encompasses montane tropical rainforest and montane cloud forest (1200 to ∼3500 m a.s.l.), as well as extensive páramo vegetation above ∼3500 m (approximately 25% of the park). There are no climatic data available for the region, but it is generally assumed that the Llanganates Cordillera is a continuously wet perhumid area, under the influence of humid air from the Amazon basin. Data from other páramo areas on the Amazonian side of the Andes indicate that annual precipitation generally exceeds 3000 mm (Rangel, 2000).


We studied an elevation gradient from 3400 to 4000 m in a remote area, approximately 27 km from the park boundary (1°10′00″S; 78°15′00″W). The gradient was within the range of what could be assumed to include the natural forest limit, extending from montane cloud forest, including the Espeletia stand within this forest, to the highest extent of the grass páramo. The latter limit was evidenced by the loss of continuous vegetation cover and the abundance of typical superpáramo species such as Loricaria ilinissae and Wemeria pygmaea (Luteyn, 1999; Sklenár and Balslev, 2004). The direct distance between the lowermost and the uppermost point along the gradient was approximately 5 km (Fig. 1), from the U-shaped valley (Valle de los Frailejones), over the lateral moraines that contained Laguna Soguillos, to an exposed rocky outcrop (Cerro Pan de Azucar) at just over 4000 m altitude.


The location of the study area within Parque Nacional Llanganates, and its location within Ecuador.


Field work was conducted in May 2000. We used a method that has been found suitable to characterize a wide range of vegetation types, including mixed rainforest and tall tussock grasslands (Dickinson et al., 1998). Six 20 × 10 m plots were randomly located at approximately 100 m intervals of altitude, where terrain permitted (time and logistical limitations unfortunately prevented plot replication). An additional plot was randomly placed in the disjunct Espeletia stand, situated on a colluvial slope at 3430 m, within the upper montane forest, the latter being recorded in the nearby (∼300 m distant) plot at 3400 m (Fig. 2). All plots were aligned with the long axis across the contour, on similar slopes (20–35°), with a generally southerly aspect. Percent cover of all vascular plant species was visually estimated in four height-life-form categories: tree (single woody stem >2 m); shrub (multi-stemmed); herb (non-woody); and ground layer (<0.5 m), apart from the stem-rosettes of Espeletia pycnophylla var. llanganatensis and Blechnum occidentale, which were recorded separately because of their distinctive and contrasting life-forms. Where species required further identification, collections were made. For the ground layer, the general cover of Sphagnum sp., and “other bryophytes,” “lichens,” litter, bare ground, and rotting stems were noted. Nomenclature follows Luteyn (1999) and Vázquez et al. (2000).

Species abundance data were analyzed using the multivariate statistical package PRIMER 5.0 (Clarke and Warwick, 2001) for community structure and composition. Cluster analyses using the group average algorithm were performed on Bray-Curtis similarity matrices derived from presence-absence and square-root transformed percent cover data to test for similarity between plant composition in the seven plots.

Soils were collected to 10 cm depth from each of the seven sites for later analyses of bulk density (dry weight per standard volume of 100 cm3), moisture content, and macronutrient composition. Two samples, each composed of five subsamples were collected systematically from each plot. On return to Quito, samples were refrigerated and later analyzed for bulk density and moisture content by means of weight difference between the field and oven-dried samples: 24 hr, 105 °C. Soil samples were visually examined for charcoal remains, indicating fire history (Di Pasquale et al., 2008). Chemical analyses were done at the Laboratoire du Sols, Institute de Réchèrche pour le Développement (IRD), France. These samples were dried for 48 hr at 30 °C and passed through a 2 mm sieve. Organic carbon and nitrogen were obtained using a CHN Carlo-Erba auto-analyser. Al, Fe, and Si were extracted with 0.2 M ammonium oxalate at pH 3 (Blakemore et al., 1981), and 0.1 M sodium pyrophosphate (Wada and Higashi, 1976), and the extracts measured by inductively coupled plasma atomic emission spectroscopy (ICP-AES). In each plot, soil temperature was also recorded at -30 cm at the time of sampling; values at this depth are likely to be stable through the day and reflect the mean annual value in these relatively thermo-stable environments (Thouret and Faivre, 1989).

To indicate microclimatic conditions at the time of the study, two data loggers were installed at 3845 m altitude on a southerly aspect from 11:30 on 8 May until 15:30 on 13 May 2000. Air temperature and humidity were recorded using a shielded Hobo H8 Pro-model, 1.5 m above ground level on the canopy fringe of a small Gynoxys acostae tree, and soil temperature at -10 cm, using an Optic Stowaway data logger.


The seven plots studied along the 600 m altitudinal gradient included a total of 105 vascular plant species and one identified bryophyte, Sphagnum magellanicum. Of the vascular plant species, there were 63 herbs, 37 erect woody species, 3 creeping shrubs, and 2 stem-rosettes (Espeletia pycnophylla var. llanganatensis and Blechnum occidentale) (Table 1). The plots with a tree cover (P2, P3, and P4) had more plant species (37–41) than those without a tree layer (P1, P5, P6, and P7; 26–30: Fig. 3). This difference in species number was mostly associated with the richer woody flora in the plots with a tree layer (14–15 woody species) compared to those without (5–9 woody species). There was no clear difference in herbaceous species richness between the plots with (20–25) and without (16–23) a tree layer. The plot with the highest overall plant richness (P4; 41 species) had the greatest number of both woody and herbaceous species.


The Espeletia pychnophylla var. llanganatensis stand within the upper Andean forest (P1) at 3430 m a.s.l. in Parque Nacional Llanganates, Ecuador.



Plant species cover in the seven quadrats sorted by occurrence along the altitudinal gradient. Shaded cells are woody species, and nonshaded cells are herbaceous species. Nonvascular categories are shown in bold. Accession numbers are shown for unidentified specimens deposited in the author's private herbarium.








There was only one plant species that occurred in all seven quadrats (Geranium sibbaldioides), and two that occurred in six plots (Neurolepis aristata and Valeriana microphylla; Table 1). On the other hand, 45 vascular species occurred in only one plot. In all plots, there was a dominance of tall, wet-condition—indicating graminoids, such as the bamboo genus Neurolepis (present in all plots as N. aristata or N. asymmetrica), Cortaderia nitida (P4, P7), Rhynchospora macrochaeta (P1, P2, P4, P5), and Luzula gigantea (P3). The characteristic páramo tussock grass, Calamagrostis intermedia, was abundant only in the two highest altitude plots (P6 and P7) above 3850 m. Dicotylous herbs attaining more than 1% cover (Valeriana plantaginae, Werneria pygmaea, and Hypochaeris sessiliflora) were also found only in the two highest plots.


Number of vascular plant species according to general life form category, for seven plots along an altitudinal transect between 3400 and 4000 m a.s.l. in an undisturbed treeline ecotone in Parque Nacional Llanganates.



Cover of tree layer and shrub layer (%) for the seven plots along an altitudinal transect between 3400 and 4000 m a.s.l. in an undisturbed treeline ecotone in Parque Nacional Llanganates.


The tree layer of the lower plots (P2, P3, and P4; Fig. 4) was composed principally of Escallonia myrtilloides and Gynoxys species. Less abundant were Myrsine dependens and Desfontainia spinosa, the latter a shrub reaching the tree layer. The shrub layer was more diverse, with Diplostephium sp., Baccharis sp., Disterigma empetrifolium, and Gaiadendron punctatum attaining considerable cover, especially in the lower plots. In the higher altitude plots, woody species either had a creeping growth form (Pernettya prostrata) or are known to tolerate (Baccharis spp., Valeriana microphylla), or be indicative of (Loricaria ilinissae), conditions associated with higher altitudes such as freezing and high irradiation (Sklenár and Balslev, 2004; Kessler et al., 2011). The change in vegetation structure along the altitudinal gradient is most clearly indicated by the decrease of the summed cover of the tree and shrub layers (Fig. 4).

The greatest floristic similarity (58%) was shown between the two highest altitude plots without a tree layer (P6 and P7). These were also the least similar to the rest (23%). Among the latter, the greatest floristic similarities were shown between P3 and P4 (at 56%) and P1 (Espeletia dominated) and P2 (closed Escallonia forest; 48%); P5 was more similar (44%) to P3 and P4 than to the other plots.

Cluster analysis of the square-root transformed percent cover data confirmed the greatest similarity to be between P6 and P7 (48%), and their differentiation from the rest of the plots (only 19% similarity). Of these, P2 (closed Escallonia forest) was least similar to the others (26%) (Fig. 5).

At an intermediate altitude along the gradient (3845 m), air temperatures over the six-day period of recording in May 2000 ranged from 0.3 to 11.5 °C, soil temperatures from 5.8 to 9.1 °C (Fig. 6), and relative humidity from 47% to 100%, but was >90% for 63% of the time. Typically, the warmest time of the day was mid-afternoon, while the coldest was variable over the period of darkness. Soil temperatures at this depth (-10 cm) were relatively stable over this period (Fig. 6). Spot soil temperatures at the more stable depth of -30 cm decreased significantly with altitude from 8.5 to 6.2 °C (r = -0.74, p < 0.01). The site at the highest elevation (P7) with a relatively open grassland was relatively warm, but this statistical relationship between temperature and altitude is driven by the temperature recorded at the Espeletia site (P7: 8.5 °C).

The soil organic C content correlated negatively with bulk density (-0.97, p < 0.01) and positively with its moisture content (0.87, p < 0.01). This intercorrelation is a common feature in mineral soils with high organic content, since organic matter is of low density and has a high water retention capacity. There was also a highly significant positive correlation (0.97, p < 0.01) between the silica content and the aluminum/iron factor (Al + 0.5Fe). There was a weaker negative correlation between altitude and %C content (and hence with soil bulk density and moisture content; r = -0.73, p < 0.01). This indicates a trend of less organic material, higher bulk density, and lower soil moisture content with increasing altitude. Soil moisture varied, but all plots were more than 60% saturated. The Al/Fe factor varied from 0.9 (P2) to 2.6 (P4), but no particular trend was obvious (Table 2). Silica was also at a maximum in P4 (6.0%) and minimum in P2 (0.6%). No charcoal was found in any sample.


This study provides a rare contemporary ecological data set for an area in the tropical high Andes that has experienced negligible human influence. Few other such studies exist (Yánez, 1998; Ramírez et al., 2009). Based on our study and wider observations of the surrounding slopes, it appears that no distinct upper forest limit occurs in this area. There was some decline in tree species richness and cover between the obvious forest plots (P1–P3: 3430–3630 m) and shrub-dominated plot 4 (subpáramo: 3700 m), with a more obvious floristic dissimilarity between this plot and plots 5–7 (open páramo: >3800 m). Thus, there was a closed forest up to ∼3600 m elevation, which graded through a narrow grass-shrub-tree dominated belt (subpáramo) of variable width but ∼200 m elevation, into grass páramo above ∼3800 m. We did not find any abrupt changes in species richness or a significant increase or decrease in species turnover at a particular altitude. Rather, turnover appeared continuous, plots displaying an essentially pair-wise pattern: the closest plots geographically, were the most similar, floristically and structurally. The lack of plot replication, however, limits interpretation. The inference of continuous turnover contrasts with findings in other transect studies in the forest-páramo ecotone by Wille et al. (2002) and Moscol (2010), who found strong species turnover around what was assumed as the original upper forest limit. The difference is most likely explained by the greater human intervention in the páramo landscape as compared to the (relatively intact) Andean forests in their study areas, while our entire study area was without apparent intervention.


Cluster analysis of square-root transformed abundance data using the Bray-Curtis similarity coefficient, from the seven plots along an altitudinal transect between 3400 and 4000 m a.s.l. in an undisturbed treeline ecotone in Parque Nacional Llanganates.



Air (1.5 m) and soil (-10 cm) temperatures (°C) recorded from 11:30 on 8 May 2000 to 15:30 on 13 May 2000 at 3845 m elevation on a southerly aspect in Parque Nacional Llanganates.


These findings lend support to the hypothesis that, in the absence of human activity, tree patches and tree individuals may occur naturally above 3500 m without having to infer a previous history of clearance, as also described by Ramírez et al. (2009). Indeed, we found no evidence of a fire history in our study area, supported by the absence of charcoal in our soil samples. The highest altitude of the closed forest (∼3600 m) in our study area is similar to that reported by Wille et al. (2002) and Jantz and Behling (2012) for other páramo sites in Ecuador, based on paleoecological studies. The observed wide gradient from forest to páramo differs from the observations of Bader et al. (2007), who described rather abrupt treelines in a comparative study on various treelines in the Andes and in Hawaii. They studied upper forest limits in mountain areas that had light to moderate anthropogenic influence, and related the abrupt upper forest limit to fire occurrence since the Holocene and positive feedback mechanisms limiting tree establishment in open páramo vegetation.

Altitude reflects a composite of environmental factors, particularly in relation to temperature and usually also precipitation. The reductions in soil organic material and moisture content, and the increase in bulk density with increasing altitude, for example, could be explained by lower primary productivity and lower litter input as temperature decreases with altitude. Of the other soil factors measured, both the silica content and the Al/Fe factor are good indicators of recent volcanic ash in the soil (Zehetner et al., 2003). There was variation along the gradient in the Al/Fe factor: at the lower altitudes (especially P2 and P3) this value was approximately 1, whereas in the higher altitude plots values were about 2, suggesting a greater influence of volcanic ash in the soil formation of the latter (Table 2). Based on the Al/Fe factor, only P4 (2.6) can technically be considered as an Andisol (FAO/ISRIC/ISSS, 1998). Thus, it could be inferred that in the lower altitude plots there is a higher proportion of weathered metamorphic rock and less pyroclastic material in the soil formation. Such an interpretation could imply a lesser influence of volcanic activity on the lower altitude systems. Our study area was also extremely wet and perhumid. The interaction between climate and soil parent material can lead to local topographic variation, which in turn influences plant community structure and composition. In our case, the most widespread taxa were of bamboo, which clearly favored the wet conditions.


Environmental data for each of the seven plots recorded in May 2000 in Parque Nacional Llanganates.


Our results can be interpreted in the general context of the wet páramo, but to what extent such patterns would be evident in drier conditions remains debatable (Stevens and Fox, 1991). Obviously, climatic conditions and plant ecophysiology are interrelated, but to what extent tree dynamics toward their upper limit are affected by wet versus dry conditions and the interactive effect with human activity and fire is open to debate (Bader, 2007; Sarmiento, 2002). Climatic variability over time also should be taken into account given environmental change and particularly the moisture fluctuations that are evident through the Holocene (Baker et ah, 2001; Marchant and Hooghiemstra, 2004).

Climatic variability, combined with the vagaries of volcanic activity, lends itself to producing some anomalous species distributions. Such may be the underlying reason behind the presence of the stand of Espeletia pychnophylla var. llanganatensis and other páramo-like vegetation on the colluvial slope within the forest in our study area. Floristically, the Espeletia stand (P1) was most similar to the nearby closed forest (P2), but only at 48%. Nevertheless, their floristic composition was more similar than to any of the other five plots. When abundance is taken into account, however, their similarity lessens and greater affinities are shown by the Espeletia stand with the mid-altitude plots (P3, P4, P5; Fig. 5) in relation to their woody/non-woody mix of vegetation. The soil temperature in the Espeletia stand indicated a relatively warm site, but the ecological significance can only be speculated from our results.

Site favorability may explain persistence of the stand at the site but not the presence of this outlier Espeletia population, 200 km south of the southernmost limit of the species' present-day continuous natural distribution between Venezuela and northern Ecuador (Monasterio and Sarmiento, 1991). We hypothesize that the past continuous distribution of this species probably extended to central Ecuador, but perhaps through volcanic activity in the Quaternary, the species was rendered extinct between northern and central Ecuador. This single Espeletia population in our study may have survived through a combination of the generally lower volcanic activity in the Llanganates area (the only non-volcanic area between northern and central Ecuador), and local site factors. Potential establishment of the Espeletia pycnophylla stand, following long-distance dispersal from the main population of the species -200 km to the north has little support, given the absence of a pappus or any other dispersal adaptation in the fruits of this genus.


Our study is one of the first to provide quantitative ecological data from a remote, continuously moist region of the tropical high Andes, apparently without the influence of human activity. The area is difficult of access and presents considerable logistical challenges, no doubt contributing to the relative lack of ecological information on such ecosystems. Our results provide baseline reference data with which to compare the impact of human activity elsewhere in the páramo region. At the least, our data give little support to there being a clear and discernible treeline under such climatic conditions. In this relatively natural setting we observed that there is a broad ecotone from montane Andean cloud forest at 3400–3600 m altitude up to open grass alpine páramo at 3800 m and above, and that within this subpáramo ecotone, there is a mosaic of scattered trees, shrubland, and grassland. This pattern is consistent with the views of Körner and Paulsen (2004), Bader et al. (2007), and Ramírez et al. (2009). Moreover, the most remote parts of Parque Nacional Llanganates present one of the last remaining reference sites in Ecuador on which to gauge the impacts of human activity. Thus, from a range of perspectives, the Parque Nacional’s ecosystems are highly significant and we encourage further research to test the hypotheses that we have raised in this paper.


The authors would like to thank Galo Medina for his great help during the field work, and Maaike Bader and Luis Daniel Llambí for reviewing our manuscript. Pascal Podwojewski arranged the soils analysis in the Institut de Recherche pour le Développement (IRD) laboratory in France, while Pascale Michel and Jacqueline Nielsen provided helpful discussion and comments on the manuscript. The field work for this study was done within the scope of the Ecuadorian Páramo Conservation Project, executed by the University of Amsterdam, Ecociencia, and the Mountain Institute, with financial support from the Royal Netherlands Embassy in Ecuador.

References Cited

  1. M. Acosta-Solis , 1984: Los páramos andinos del Ecuador. Quito: Publicaciones MAS, 220 pp. Google Scholar
  2. C. Ange Jaramillo , C. Castaño Uribe , F. Arjona Hincapié , J. V. Rodriguez , and C. L. Durán , 2002: Congreso Mundial de Páramos. Memorias. Bogotá: Ministerio del Medio Ambiente, CAR, IDEAM, Conservation International, 1185 pp. Google Scholar
  3. J. J. Anhalzer , 1998: Llanganati. Quito: Libri Mundi. 97 pp. Google Scholar
  4. M. Y. Bader , 2007: Tropical Alpine Treelines: How Ecological Processes Control Vegetation Patterns and Dynamics. Ph.D. thesis, Wageningen, Wageningen University, 193 pp. Google Scholar
  5. M. Y. Bader , M. Rietkerk , and A. K. Bregt , 2007: Vegetation structure and temperature regimes of tropical alpine treelines. Arctic, Antarctic, and Alpine Research 39: 353–364. Google Scholar
  6. P. A. Baker , G. O. Seltzer , S. C. Fritz , R. B. Dunbar , M. J. Grove , P. M. Tapia , S.L. Cross , H. D. Brown , and J. P. Broda , 2001: The history of South American tropical precipitation for the past 25,000 years. Science , 291: 640–643. Google Scholar
  7. L. C. Blakemore , P L. Searle , and B. K. Daly , 1981: Methods for Chemical Analysis of Soils. Wellington: New Zealand Soil Bureau, Scientific Report 80, 103 pp. Google Scholar
  8. W. Buytaert , R. Célleri , B. De Bièvre , F. Cisneros , G. Wyseure , J. Deckers , and R. Hofstede , 2006: Human impact on the hydrology of the Andean páramos. Earth-Science Reviews , 79: 53–72. Google Scholar
  9. W. Buytaert , and De Bièvre B. , 2012: Water for cities: the impact of climate change and demographic growth in the tropical Andes. Water Resources Research , 48: W08503. Google Scholar
  10. A. Cabaneiro , I. Fernandez , L. Pérez-Ventura , and T. Carballas , 2008: Soil CO2 emissions from Northern Andean páramo ecosystems: Effects of fallow agriculture. Environmental Science and Technology , 42: 1408–1415. Google Scholar
  11. C. Castaño 2002: Páramos y ecosistemas alto andinos de Colombia en condición hotspot y global climatic tensor. Bogotá: IDEAM. Google Scholar
  12. R. A. Chimner , and J. M. Karberg , 2008: Long-term carbon accumulation in two tropical mountain peatlands, Andes Mountains, Ecuador. Mires and Peat , 3: art 4. Google Scholar
  13. K. R. Clarke , and R. M. Warwick , 2001: Change in Marine Communities: An Approach to Statistical Analysis and Interpretation. 2nd edition. Plymouth: Primer-E, 172 pp. Google Scholar
  14. A. M. Cleef , 1981: The Vegetation of the Páramos of the Colombian Cordillera Oriental. Vaduz, Liechtenstein: J. Cramer. 321 pp. Google Scholar
  15. D. A. Contreras , 2010: Landscape and environment: insights from the prehispanic Central Andes. Journal of Archaeological Research , 18: 241–288. Google Scholar
  16. J. Cuatrecasas , 1958: Aspectos de la vegetación natural de Colombia. Revista de la Academia Colombiana de Ciencias Exactas y Físicas , 10: 221–264. Google Scholar
  17. J. Cuatrecasas , 2013: A Systematic Study of the Subtribe Espeletiinae (Heliantaceae, Asteracea). New York: NYBG Press, Memoirs of the New York Botanical Garden, Volume 107, 704 pp. Google Scholar
  18. F. Cuesta , M. Bustamante , M. T. Becerra , J. Postigo , and M. Peralvo , 2012 : Panorama andino de cambio climático: vulnerabilidad y adaptación en los Andes Tropicales. Lima: Condesan, SG-CAN, 329 pp. Google Scholar
  19. G. Di Pasquale , M. Marziano , S. Impagliazzo , S. Lubritto , A. De Natale , and M. Y. Bader , 2008: The Holocene treeline in the northern Andes (Ecuador): First evidence from soil charcoal. Palaeogeography, Palaeoclimatology, Palaeoecology , 259: 17–34. Google Scholar
  20. K. J. M. Dickinson , A. F. Mark , B. I. P. Barratt , and B. H. Patrick , 1998: Rapid ecological survey, inventory and implementation: a case study from Waikaia Ecological Region, New Zealand. Journal of the Royal Society of New Zealand , 28: 83–156. Google Scholar
  21. H. Ellenberg , 1958: Wald oder Steppe. Die natüraliche Planzendecke der Anden Perus (I, II). Die Umschau im Wissenschaft und Technik , 21: 679–681, 22: 679–681. Google Scholar
  22. H. Ellenberg , 1979: Man's influence on tropical mountain ecosystems in South America. Journal of Ecology , 67: 401–416. Google Scholar
  23. FAO/ISRIC/ISSS, 1998: World Reference Base for Soil Resources. Rome: FAO, World Soil Resources Report. Volume 84, 88 pp. Google Scholar
  24. K. A. Farley E. G. Jobbágy R. B. Jackson , 2005: Effects of afforestation on water yield: a global synthesis with implications for policy. Global Change Biology , 11: 1565–1576. Google Scholar
  25. K. A. Farley , E. F. Kelly , and R. G. M. Hofstede , 2004: Soil organic carbon and water retention after conversion of grasslands to pine plantations in the Ecuadorian Andes. Ecosystems , 7: 729–739. Google Scholar
  26. M. J. Germino , and W. K. Smith , 1999: Sky exposure, crown architecture, and low-temperature photoinhibition in conifer seedlings at alpine treeline. Plant, Cell, and Environment , 22: 407– 415. Google Scholar
  27. W. González , D. L. Llambí , and J. K. Smith , 2011: Dinámica sucesional del componente arbóreo en la transición entre el bosque-páramo en los Andes Tropicales. Ecotrópicos , 24: 60–79. Google Scholar
  28. G. Grabherr , M. Gottfried , and H. Pauli , 2010: Climate change impacts in alpine environments. Geography Compass , 4: 1133– 1153. Google Scholar
  29. J. Grace , F. Berninger , and L. Nagy , 2002: Impacts of climate change on the tree line. Annals of Botany , 90: 537–544. Google Scholar
  30. R. G. M. Hofstede . 1995: Effects of livestock farming and recommendations for management and conservation of páramo grasslands (Colombia). Land Degradation and Rehabilitation , 6: 133–147. Google Scholar
  31. R. G. M. Hofstede , J. P. Groenendijk , R. Coppus , J. Fehse , and J. Sevink , 2002: Impact of pine plantations on soils and vegetation in the Ecuadorian high Andes. Mountain Research and Development , 22: 159–167. Google Scholar
  32. R. Hofstede , P. Segarra , and P. Mena Vásconez , 2003: Los páramos del mundo. Quito: IUCN, Global Peatland Initiative, Ecociencia, 299 pp. Google Scholar
  33. R. Hofstede, 2011: Historia, tendencias y perspectivas para el manejo de los páramos. In G. Maldonado , and B. de Bievre (eds.), PARAMUNDI, 2do Congreso Mundial de Páramos. Memorias. Lima: CONDESAN, 34–45. Google Scholar
  34. J. L. Innes , 1991: High-altitude and high-latitude tree growth in relation to past, present and future global climate change. Holocene , 1: 168–173. Google Scholar
  35. N. Jantz , and H. Behling , 2012: A Holocene environmental record reflecting vegetation, climate, and fire variability at the Páramo of Quimsacocha, southwestern Ecuadorian Andes. Vegetation History andArchaeobotany , 21: 169–185. Google Scholar
  36. P. M. Jørgensen , and Ulloa Ulloa , C. , 1994: Seed Plants of the High Andes of Ecuador: A Checklist. Aarhus: Department of Systematic Botany, Aarhus University, AAU Report 34, 453 pp. Google Scholar
  37. M. Kessler , J. A. Grytnes , S. R. P. Halloy , J. Kluge , T. Krömer , B. León. , M. J. Macía , and K. R. Young , 2011: Gradients of plant diversity: local patterns and processes. In S. K. Herzog , R. Martinez , P. M. Jørgensen , and H. Tiessen (eds.), Climate Change and Biodiversity in the Tropical Andes. Sao José dos Campos, Brazil: IAI-SCOPE, 204–219. Google Scholar
  38. C. Körner , 1998: A re-assessment of high elevation treeline positions and their explanation. Oecologia , 115: 445–459. Google Scholar
  39. Ch. Körner , and E. Spehn , 2002: Mountain Biodiversity: A Global Assessment. New York: Parthenon, 341 pp. Google Scholar
  40. C. Körner , and J. Paulsen , 2004: A world-wide study of high altitude treeline temperatures. Journal of Biogeography , 31: 713–732. Google Scholar
  41. C. Körner , 2012: Alpine Treelines: Functional Ecology of the Global High Elevation Tree Limits. Basel, Switzerland: Springer, 220 pp. Google Scholar
  42. S. Laegaard , 1992: Influence of fire in the grass páramo vegetation of Ecuador. In H. Balslev , and J. L. Luteyn (eds.), Páramo: An Andean Ecosystem under Human Influence. London: Academic Press, 151– 170. Google Scholar
  43. W. Lauer , 1981: Ecoclimatological conditions of the pàramo belt in the tropical high mountains. Mountain Research and Development , 1: 209–221. Google Scholar
  44. L. D. Llambí , J. A. Puentes , and C. Garcia-Núñez , 2013: Spatial relations and population structure of a dominant tree along a treeline ecotone in the Tropical Andes: interactions at gradient and plant-neighbourhood scales. Plant Ecology & Diversity , 6: 343–353. Google Scholar
  45. M. E. López Sandoval , 2004: Agricultural and Settlement Frontiers in the Tropical Andes: The Páramo Belt of Northern Ecuador, 1960–1990. Regensburg, Germany: University of Regensburg, Regensburger Geographische Schriften, Heft 37, 180 pp. Google Scholar
  46. J. L. Luteyn , 1999: Páramos. A Checklist of Plant Diversity, Geographical Distribution and Botanical Literature. New York: The New York Botanical Garden Press, Memoirs of the New York Botanical Garden, Volume 84, 278 pp. Google Scholar
  47. R. Marchant , and H. Hooghiemstra , 2004: Rapid environmental change in African and South American tropics around 4000 years before present: a review. Earth Science Reviews , 66: 217–260. Google Scholar
  48. G. Miehe , and S. Miehe , 1994: Zur oberen Waldgrenze in tropischen Gebirge. Phytocoenologia , 24: 53–110. Google Scholar
  49. G. Miehe , and S. Miehe , 2000: Comparative high mountain research on the treeline ecotone under human impact. Carl Troll's “asymmetrical zonation of the humid vegetation types of the world” of 1948 reconsidered. Erdkunde , 54: 34–50. Google Scholar
  50. M. Monasterio , and L. Sarmiento , 1991: Adaptive radiation of Espeletia in the cold Andean tropics. Trends in Ecology and Evolution , 6: 387–391. Google Scholar
  51. M. C. Moscol , 2010: Holocene Upper Forest Line Dynamics in the Ecuadorian Andes. Ph.D. dissertation. Amsterdam: University of Amsterdam, 228 pp. Google Scholar
  52. P. Mothes , 1991: El paisaje volcánico de la Sierra Ecuatoriana. Geomorfología, fenómenos volcánicos y recursos asociados. Quito: Corporación Editora Nacional/Colegio de Geógrafos del Ecuador. Estudios de Geografía, 4, 92 pp. Google Scholar
  53. P. Podwojewski , J. Poulenard T. Zambrana , and R. Hofstede , 2002: Overgrazing effects on vegetation cover and volcanic ash soil properties in the páramo of Llangahua and La Esperanza (Tungurahua, Ecuador). Soil Use and Management , 18: 45–55. Google Scholar
  54. M. Price , 2006: Global Change in Mountain Regions. Duncow, U.K.: Sapiens, 343 pp. Google Scholar
  55. L. Ramírez , L. D. Llambí , T. Schwarzkopf , L. E. Gámez , and N. J. Márquez , 2009: Vegetation structure along the forest-páramo transition belt in the Sierra Nevada de Mérida: implications for understanding treeline dynamics. Ecotrópicos , 22: 83–98. Google Scholar
  56. C. J. O. Rangel , 2000: Colombia Diversidad Biológica III. La region de vida paramuna. Bogotá: Universidad Nacional de Colombia, Instituto de Ciencias Naturales, Instituto Alexander von Humboldt, 902 pp. Google Scholar
  57. A. P. Smith , 1994: Introduction to tropical alpine vegetation. In P. W. Rundel , A. P. Smith , and F. C. Meinzer (eds.), Tropical Alpine Environments. Plant Form and Function. Cambridge: Cambridge University Press, 1–19. Google Scholar
  58. S. Salamanca , 1992: La vegetación del páramo y su dinámica en la macizo volcánico Ruiz-Tolima (Cordillera Central, Colombia). Bogotá: Instituto Geográfico Augustin Codazzi, Análisis Geográficos, 21. 155 pp. Google Scholar
  59. F. O. Sarmiento , 2002: Human drivers of landscape change: treeline dynamics in neotropical montology. Ecotropicos , 15: 129–146. Google Scholar
  60. P. Sklenár , and H. Balslev , 2004: Superpáramo plant species diversity and phytogeography in Ecuador. Flora , 200: 416–433. Google Scholar
  61. A. P. Smith , 1978: Establishment of seedlings of Polylepis sericea in the páramo (Alpine) zone of the Venezuelan Andes. Bartonia , 45: 11–14. Google Scholar
  62. G. C. Stevens , and J. F. Fox , 1991: The causes of treeline. Annual Review of Ecology and Systematics , 22: 177–191. Google Scholar
  63. F. H. Tonneijck , J. Van Der Plicht , B. Jansen , J. M. Verstraten , and H. Hooghiemstra , 2006: Radiocarbon dating of soil organic matter fractions in Andosols in northern Ecuador. Radiocarbon , 48: 337– 353. Google Scholar
  64. J. C. Thouret , and P. Faivre , 1989: Suelos de la Cordillera Central. In T. Van der Hammen , S. Diaz Piedrahita , and V. J. Alvarez (eds.). La Cordillera Central Colombiana. Transecto Parque los Nevados (segunda parte). Estudios de Ecosistemas Tropandinos, 3. Berlin/ Stuttgart: J. Cramer, 293–442. Google Scholar
  65. C. Ulloa Ulloa , and Jørgensen , P. , 1993: Árboles y arbustos de los Andes del Ecuador. AAU Reports 30. Aarhus, Denmark: Department of Systematic Botany, Aarhus University, 264 pp. Google Scholar
  66. M. A. Vázquez , M. Larrea , and L. Suárez , 2000: Biodiversidad en el Parque Nacional Llanganates: un reporte de las evaluaciones y socioeconómicas rápidas. Quito: EcoCiencia, Ministerio del Ambiente, Herbario Nacional del Ecuador, Museo Ecuatoriana de Ciencias Naturales, Instituto Internacional de Reconstrucción Rural, 203 pp. Google Scholar
  67. V. Vélez , J. Cavelier , and B. Devia , 1998: Ecological traits of the tropical treeline species Polylepis quadrijuga (Rosaceae) in the Andes of Colombia. Journal of Tropical Ecology , 15: 771–787. Google Scholar
  68. P. A. Verweij , 1995: Spatial and Temporal Modelling of Vegetation Patterns. Burning and Grazing in the Páramo of Los Nevados National Park, Colombia. Ph.D. dissertation. Amsterdam: University of Amsterdam, 233 pp. Google Scholar
  69. K. Wada , and T. Higashi , 1976: The categories of aluminium- and iron-humus complexes in ando soils determined by selective dissolution. Journal of Soil Science , 27: 357–368. Google Scholar
  70. H. Walter , and E. Medina , 1969: La temperatura del suelo como factor determinante para la caracterización de los pisos subalpino y alpino en los Andes de Venezuela. Boletín de la Sociedad Venezolana de Ciencias Naturales , 28: 201–210. Google Scholar
  71. P. Wardle , 1971: An explanation for alpine timberline. New Zealand Journal of Botany , 9: 371–402. Google Scholar
  72. M. Wille , H. Hooghiemstra , R. Hofstede , J. Fehse , and J. Sevink , 2002: Upper forest line reconstruction in a deforested area in northern Ecuador based on pollen and vegetation analysis. Journal of Tropical Ecology , 18:409–440. Google Scholar
  73. P. Yánez , 1998: Caracterización florística en un sector de cambio páramo-selva nublada en el Parque Nacional Sierra Nevada, Venezuela. Revista Forestal Venezolana , 42: 51–62. Google Scholar
  74. K. R. Young , and P. L. Keating , 2001: Remnant forests of Volcán Cotacachi, northern Ecuador. Arctic, Antarctic, and Alpine Research , 33: 165–172. Google Scholar
  75. K. R. Young , and B. León , 2007: Tree-line changes along the Andes: implications of spatial patterns and dynamics. Philosophical Transactions of the Royal Society B , 362: 263–272. Google Scholar
  76. K. R. Young , 2009: Andean land use and biodiversity: humanized landscapes in a time of change. Annals of the Missouri Botanical Garden , 96: 492–507. Google Scholar
  77. F. Zehetner , W. P. Miller , and L. T. West , 2003: Pedogenesis of volcanic ash soils in Andean Ecuador. Journal of the Soil Science Society of America , 67: 1797–1809. Google Scholar
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Robert G. M. Hofstede, Katharine J. M. Dickinson, Alan F. Mark and Edwin Narváez "A Broad Transition from Cloud Forest to Páramo Characterizes an Undisturbed Treeline in Parque Nacional Llanganates, Ecuador," Arctic, Antarctic, and Alpine Research 46(4), (1 November 2014).

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