Translator Disclaimer
1 February 2011 Vegetation Development on Deglaciated Rock Outcrops from Glaciar Frías, Argentina
Author Affiliations +
Abstract

The retreat of glaciers during past decades has led to the emergence of large rock outcrops in many glaciated areas around the world. Primary succession of vegetation in glacier forelands has been described for many regions, but most studies have been conducted on glacial deposits, whereas deglaciated rock outcrops have received little attention. This study assesses the pattern of primary succession on a chronosequence of five rock outcrops exposed during the past 140 years by the retreat of Glaciar Frías in the Patagonian Andes, Argentina. Data on floristic composition and species cover for algae, lichens, ferns, bryophytes, and vascular plants were recorded on sampling plots. Ordination and classification analyses discriminate three major successional stages, each dominated by a different species assemblage, suggesting directional replacement of species in the succession. The pioneer stage is dominated by the crustose lichen Placopsis perrugosa, the mid-successional stage by a lichen-moss mat dominated by the moss Racomitrium lanuginosum, and the late-successional stage by a large diversity of vascular plants. The low density of Nothofagus dombeyi saplings in the late-successional site indicates that plant succession is still in progress 140 years after deglaciation. Progress in succession appears to be influenced by species life-cycle traits and facilitative interactions among species. The comparison of the successional processes between rock outcrops and unconsolidated glacial deposits suggests that the vegetation sequence is similar, but the rate of succession is slower on rock outcrops. The development of a ground lichen-moss cover, previous to the widespread colonization by vascular plants, accounts for the slower succession progress on rock outcrops. The establishment of Nothofagus stands takes at least 100 yrs longer on the rock outcrops than on glacial deposits. Under predicted climate warming, most Patagonian Andes glaciers will continue the retreat along steep bedrock slopes, where similar, long-term vegetation successional patterns to those observed on Glaciar Frías foreland will eventually occur.

Introduction

Climatic warming in mountain ecosystems influences the dynamics of the vegetation through changes in ecophysiological processes and in disturbance regimes (Körner, 2005). In addition, climatic warming affects glaciated-mountain ecosystems by determining glacier retreat that exposes extended areas of bare terrain to biological colonization (Matthews and Whittaker, 1987; Chapin et al., 1994). Studies of ecosystem development on recently deglaciated terrains in Europe and North America provide comprehensive information on successional vegetation changes and the mechanisms driving succession (Matthews, 1992). The relative importance of vegetation traits, biological interactions, and environmental forces driving the processes of species colonization and replacement are well known (Svoboda and Henry, 1987; Walker and Chapin, 1987; Chapin et al., 1994). In addition, it has been shown that landscape characteristics, stochastic processes, and disturbance events have a large influence on vegetation successional patterns (del Moral et al., 1995; Matthews, 1999).

Large rock outcrops have emerged during past decades from beneath glaciers in many glacierized areas, such as Patagonia, the Alps, and North America (Rivera and Casassa, 2004; Paul et al., 2007; Pelto, 2009). Most studies of primary succession on deglaciated terrains have been performed on unconsolidated glacial sediments, whereas there is little empirical data on vegetation development on bedrock outcrops (Matthews, 1992). Rock outcrops are stressful environments subjected to high thermal contrasts, drought due to low water holding capacity, substrate instability due to intense water runoff, and limiting soil formation (Shure and Ragsdale, 1977; Sarthou et al., 2009). Our knowledge about the primary succession on rock outcrops is mainly based on studies conducted within forested landscapes. In general, the vegetation establishment on outcrops is initiated by the early development of a lichen cover and an organic matter layer, and the succession progress is frequently associated with the deepening of the soil layer (Burbanck and Phillips, 1983; Uno and Collins, 1987; Asselin et al., 2006). The development of a mature forest community on rock outcrops is slow and periods of ca. 1000 years have been reported (Asselin et al., 2006). A similar slow vegetation development occurs on lava flows, where the pioneer cryptogam colonizers are replaced by higher plants ca. 600 years after the lava emplacement (Cutler et al., 2008). Hence, successional processes involving interactions between different vegetation groups are expected to occur on long-term temporal scales on deglaciated rock outcrops. Additional analyses on deglaciated rock outcrops are required to properly understand the landscape changes related to glacier retreat along mountain bedrock slopes, and to predict short- and long-term effects of changing climate on glaciated-mountain ecosystems.

The retreat of glaciers is a conspicuous sign of climate changes during the last century in the Patagonian Andes (Luckman and Villalba, 2001; Masiokas et al., 2010), yet investigations of primary succession on recently deglaciated terrains have been relatively rare in this area. Some studies have analyzed the vegetation on glacier moraines (Lawrence and Lawrence, 1959; Heusser, 1960, 1964; Pisano, 1978; Rabassa et al., 1981; Veblen et al., 1989; Dollenz, 1991; Armesto et al., 1992) and the influence of some specific biological interactions on plant colonization (Henríquez, 2004; Henríquez and Lusk, 2005). These studies have mostly focused on Nothofagus establishment and have rarely considered other components of the vegetation, such as algae, lichens, and bryophytes. Moreover, the study of the primary succession in general has received little attention within Nothofagus forests in the southern hemisphere (Orwin, 1972; Archer et al., 1973; Ashton and Moore, 1978; Wardle, 1980; Sommerville et al., 1982).

The aim of this study is to document and assist understanding of the primary succession process on rock outcrops following glacier retreat. Glaciar Frías, in the north Patagonian Andes, offers an excellent opportunity for the study of vegetation succession on rocky environments. Five rock outcrops have been exposed by glacier recession from its Neoglacial maximum and provide a chronosequence of sites covering the last 140 years (Fig. 1). In this paper we describe the pattern of primary succession of vegetation on the Glaciar Frías outcrops and infer the possible mechanisms driving vegetation development in these stressful environments. The study integrates all vegetation groups (algae, lichens, ferns, mosses, and vascular plants) allowing a thorough analysis of the community changes over time. In addition, successional pattern on rock outcrops at Glaciar Frías were compared with vegetation establishment on unconsolidated glacial deposits reported in the literature for the Patagonian Andes. By conducting this analysis we explore possible future vegetation landscape changes in mountain regions as glaciers continue retreating along bedrock slopes.

FIGURE 1

Location map of Glaciar Frías foreland in the north Patagonian Andes showing the position of the frontal moraines (M) and the sampling sites (S). Estimated dates of moraines and sampling sites exposition are given in Table 1.

i1523-0430-43-1-35-f01.tif

Methods

STUDY AREA

Glaciar Frías is the northernmost ice body of Mount Tronador (41°10′S, 71°50′W), one of the highest mountains (3554 m) in the northern Patagonian Andes (Fig. 1). The climate of the zone is temperate and wet. Available climatic data from the Mascardi weather station, 20 km east from Glaciar Frías, indicate a mean annual temperature of 7.6 °C (January mean 12.9 °C, July mean 2.4 °C). Total annual precipitation in the Frías valley is ca. 4300 mm (Barros et al., 1983; Villalba et al., 1990). The vegetation in the Frías valley corresponds to the Valdivian temperate rain forest, which is a multistratified forest dominated by the evergreen Nothofagus dombeyi and the conifer Fitzroya cupressoides (Ezcurra and Brion, 2005).

The chronology of Glaciar Frías recession is well known from the study of historical drawings, written records, terrestrial and aerial photographs, direct measurements of ice front, and the dendrochronological dating of moraines. The maximum Neoglacial advance of Glaciar Frías was reached ca. ad 1660 (Rabassa et al., 1978; Villalba et al., 1990), and the glacier has subsequently retreated more than 1500 m along the Frías valley (Fig. 1). A sharp forest trim-line defines the boundary between the glacier foreland and the mature forest not affected by the last major Neoglacial advance. A well-preserved sequence of frontal moraines remains in the bottom of the valley as evidence of seven minor readvances of Glaciar Frías since the last Neoglacial maximum (Villalba et al., 1990; Masiokas, 2008). The most recent readvance occurred during the years 1976–1977 (Rabassa et al., 1979).

At the Glaciar Frías foreland the bottom and slopes of the valley show contrasting environments. Along the bottom of the Frías valley wet meadows cover the glaciofluvial deposits and vascular plants grow on the frontal moraines. In contrast, along the valley slopes, bedrock outcrops without glacial sediments on top are mostly covered by lichens and bryophytes with sparsely distributed vascular plants. Inclination of the valley slopes is around 30°.

The study sites are located on the southern valley side, where five granodiorite rock outcrops have been successively exposed by the retreat of Glaciar Frías (Fig. 1). Exposure dates for the rock outcrops were estimated from the dates of the moraines (Villalba et al., 1990; Masiokas, 2008), direct measurements of ice front positions (Rabassa et al., 1978), and the analysis of old terrestrial and aerial photographs (Fig. 2). Study sites were located between points of known exposure times, so the mean of these dates was used as an estimation of the sampling site age. The five rock outcrops studied are a chronosequence covering the past 140 years (Table 1). As the glacier forefield represents a spatial chronosequence, the analysis of the vegetation growing on sites exposed at different ages was used to infer the process of primary succession (Pickett, 1989; Foster and Tilman, 2000; Walker et al., 2010).

FIGURE 2

Selected historical photographs and drawings of Glaciar Frías used to constrain the exposure dates of the rock outcrops in the study sites. Historical sources: (a) Fonck (1896), (b) Steffen (1909), (c) De Agostini (1945), (d) anonymous (IANIGLA archive), (e and f) R. Villalba.

i1523-0430-43-1-35-f02.tif

TABLE 1

Exposure dates for sampling sites estimated from historical information and dendrochronological dating of frontal moraines. Historical information includes: TP (terrestrial photographs), AP (aerial photographs), D (drawings), and FP (direct measurement of glacier front positions). The historical drawing by Hess in 1856 and the terrestrial photos are shown in Figure 2. Dates of moraines from Villalba et al. (1990).

i1523-0430-43-1-35-t01.tif

SAMPLING DESIGN

Rock outcrops are characterized by high compositional heterogeneity in vegetation due to the presence of a large variety of microhabitats modulated by topography (Wiser et al., 1996; Matthes-Sears and Larson, 2006; Opazo Medina et al., 2006). The rock outcrops exhibit meso- and micro-scale topographic variability due to the presence of drainage channels between outcrops and small cracks on the rock surface, respectively. Inspection of the area evidences striking differences in vegetation between rock surfaces and drainage channels. However, drainage channels constitute a minor fraction of the Glaciar Frías rock outcrop landscape. In consequence, our study focused in the analysis of the vegetation growing on the rock surfaces, the major landscape features on the deglaciated valley slopes.

We randomly located 10 sampling plots in each study site. Plots of 5 × 10 m were used for analyzing ferns and vascular plants, and subplots of 1 × 1 m for analyzing the cryptogamic flora (algae, lichens, ferns, and bryophytes). Within each plot and subplot the species were recorded and their coverage visually estimated. Cover estimates for lichens and bryophytes were recorded to the species level whenever possible or by genera or morphological groups when field identification was not feasible. In addition, a floristic inspection throughout the study area was conducted to detect the presence of species not occurring in the plots. Lichens and mosses not identified in the field were collected for later taxonomical determination in the laboratory. Voucher specimens are deposited at the Argentinean Institute of Snow, Ice and Environmental Sciences (IANIGLA). Nomenclature for vascular plants follows Zuloaga and Morrone (1999a, 1999b), and for lichens and bryophytes Brummitt and Powell (1992).

Altitude, aspect, slope, surface topography, canopy coverage, percentage of the substrate covered by pebbles, and percentage of bare rock outcrop and bare soil were recorded at each plot. Surface topography was categorized as elevated, depressed, and flat with respect to the surrounding area. Inclination of the sampling plots depends on microtopography, and the slope at each sampling plot was estimated using clinometers. Percent canopy coverage was estimated using a spherical densitometer.

DATA ANALYSES

Patterns of variation in plant diversity along the successional sequence were assessed using indices of species diversity and plots of the species-abundance distribution (Lambshead et al., 1983; Magurran, 1988). Three diversity indices which provide complementary information on community structure were selected: the Shannon index (H′) combines species richness and evenness; the reciprocal of Simpson's index (1/D) measures species dominance depending on the proportional abundance of all species; and the Berger-Parker index gives a value of dominance of the most abundant species, dividing the coverage of the dominant species by the total coverage of the species.

The vegetation data were analyzed by Detrended Correspondence Analysis (DCA), which ordinates sampling plots according to their floristic composition and species coverage, allowing assessment of overall patterns in vegetation changes (Jongman et al., 1995). The ordination matrix contained 71 species in 50 sampling plots. Detrending was performed by segments, and rare species were not down-weighted. Vegetation data were also analyzed using a Two-Way Indicator Species Analysis (TWINSPAN) in order to determine vegetation groups (VG) characteristic of the different successional stages (Leps and Šmilauer, 1999). This analysis works with qualitative data, so quantitative data of species coverage was transformed to qualitative variables called pseudospecies, which are defined by cut-levels of species coverage (Jongman et al., 1995). In our analysis pseudospecies cut levels were set at 0, 2, 5, 20 and 50%, representing the whole range of species coverage. The minimum group size for division was 7, and a maximum of 4 levels of division was used.

The influence of different variables on vegetation changes were indirectly assessed correlating the DCA ordination axes with the dates of site exposure and environmental variables. In addition, a Canonical Correspondence Analysis (CCA) was applied to directly assess the main patterns of variation in the vegetation community accounted for by the explanatory variables (Jongman et al., 1995). The variables included were site exposure date, slope, surface topography, canopy coverage, and percentage of bare rock outcrop, bare soil, and pebbles. A Monte Carlo permutation test was used to test the significance of the first ordination axis (Leps and Šmilauer, 1999). In addition, the statistical significance of the partial effect of each explanatory variable (variability explained by a given variable after accounting for the effects of the other variables under analysis) was estimated by a Monte Carlo permutation test as the respective variable was step-wise added to the model.

Results

GENERAL PATTERNS IN SPECIES RICHNESS, COVER, AND DIVERSITY

A total of 97 species were identified in the floristic surveys performed on the rock outcrops studied at Glaciar Frías foreland. These include species from 10 different life forms, trees; shrubs; herbs; graminoid herbs; ferns; mosses; foliose, fruticose, and crustose lichens; and algae (the full list of species is available from the corresponding author upon request). Fourteen additional species (9 graminoid herbs, 2 mosses, and 3 crustose lichens) were not identified due to the absence of reproductive structures at the time of sampling.

A general pattern of increasing species numbers and total plant cover occurred along the spatial chronosequence (Table 2). From the youngest to the oldest site (sites 1 to 5) the number of species increased from 31 to 44 and total plant cover increased from 44 to 154%, respectively. In the earliest exposed sites, total plant cover exceeded 100% due to the development of a multistratified community. Crustose lichens dominate the recently exposed sites (sites 1 to 3), but decline in the oldest sites 4 and 5. Cover of vascular plants, mosses, and foliose and fruticose lichens gradually increase with age. Ferns and algae are poorly represented at the study outcrops.

TABLE 2

Community structure in the five study sites along the Glaciar Frías forefield: mean ± standard deviation cover of each vegetation group and diversity indices. Estimated exposure dates of sites are given in Table 1; site 1 is the youngest and site 5 the oldest.

i1523-0430-43-1-35-t02.tif

The species-abundance distributions at each study site are shown in Figure 3. The curves for all five sample sites indicate the presence of one or two dominant species (>10% cover), a variable number of species with intermediate abundance (between 1 and 10% cover), and a large number of rare species (<1% cover). Dominance increases over time, as indicated by the steep initial portions of the species rank-abundance curves, but there is also a general trend of increasing diversity through the successional sequence, with higher species richness and more even distribution of abundance among the species of intermediate abundance (Fig. 3). Interpretation of the species diversity indices is problematic because the rank-abundance curves from sites 2, 3, and 4 intersect each other, indicating that these communities are not comparable in terms of intrinsic diversity (Lambshead et al., 1983). Comparison of the species diversity indices for the oldest site 5 and the earlier site 1 (their rank-abundance curves do not intersect; Fig. 3) agree with the interpretation of the rank-abundance curves suggesting a trend of increasing species diversity in the vegetation community and of dominance of the most abundant species as succession progresses (Table 2).

FIGURE 3

Species-abundance distribution plots for each study site. Site 1 is the youngest and site 5 the oldest.

i1523-0430-43-1-35-f03.tif

VEGETATION ASSEMBLAGES

The species classification by TWINSPAN differentiated six major vegetation assemblages. Based on the time of entering in the successional sequence and the period in which a species achieves the maximum coverage, the vegetation assemblages were differentiated as corresponding to the pioneer, mid-, or late-successional stage (Table 3). The pioneer species are those that colonized the recently exposed sites but disappeared in older sites, the mid-successional species prevailed in the middle-aged sites, whereas the late-successional species appear late in the succession.

TABLE 3

Mean percent cover (%) of the species in the five study sites at Glaciar Frías foreland. Cover values higher than 1.5% are indicated in bold. Vegetation groups (VG) as defined by TWINSPAN. Estimated exposure date of sites is given in Table 1.

i1523-0430-43-1-35-t03.tif

The pioneer species dominate the community for about 50 years (sites 1 and 2) and decrease in coverage later in the succession (Table 3). The dominant species in the pioneer-successional stage are the crustose lichen Placopsis perrugosa, forming a dense cover on the rock outcrops, and the moss Andreaea sp., growing in small cracks on the rock surfaces. Besides these, the lichens Stereocaulon speciosum and Placopsis stenophylla, the moss Racomitrium lanuginosum, and the small shrubs Senecio argyreus, Baccharis racemosa, and Gaultheria pumila are also present with relatively high coverage in the early stage (Table 3). A large diversity of vascular plants (classified in the VG1) colonizes early the fine material accumulated between rock outcrops (Table 3). Most of these vascular species are only sporadically present in the younger and not in the older sites, thus we assumed that they are present by chance and not actually part of the successional sequence on the rock outcrops. Indeed, ordination analysis of the composition and coverage data shows that these species are clearly separated in the right side of the ordination graph, outside the center of the diagram where the sample sites lie (Fig. 4), indicating a minor influence of VG1 plants on the sites ordination.

FIGURE 4

Results of the canonical correspondence analysis (CCA) of species and samples. (top) Ordination of sampling plots and explanatory environmental variables. The quantitative environmental variables are shown by vectors and the variable topography as centroids of each category. (bottom) Ordination of species. Species are differentiated as: □ Pioneer, • Mid-successional and ▴ Late-successional, according to their classification in the TWINSPAN analysis. Species abbreviations are given in Table 3. Eigenvalues for the first and second axes are 0.364 and 0.163, respectively.

i1523-0430-43-1-35-f04.tif

The mid-successional stage is dominated by the moss R. lanuginosum. This species became prominent about 80 years after site exposure (site 3), and in combination with the fruticose lichens Stereocaulon spp., Cladonia lepidophora, and C. subchordalis forms a dense lichen-moss carpet on the rock surfaces (Table 3). After about 140 years the lichen-moss mat covered more than 90% of the rock surface on site 5. Other characteristic species of the mid-successional stage were the shrubby vascular plants Gaultheria pumila and G. caespitosa. In addition, species typical of the pioneer and late-successional stages, such as Senecio argyreus and Escallonia alpina, respectively, were present with relatively high coverage in middle-aged sites (Table 3).

The late-successional stage is characterized by the invasion of a large diversity of vascular plant species, which on average contribute 47.2% of the total vegetation cover (Tables 2 and 3). Local variability in vegetation development is high, as indicated by the large standard deviation of the mean cover values for the vegetation groups (Table 2). The most relevant vascular plants, in order of their coverage are Empetrum rubrum, Berberis buxifolia, Quinchamalium chilense, Discaria nana, Escallonia alpina, Baccharis racemosa, and some graminoid herbs.

VEGETATION PATTERNS AND EXPLANATORY VARIABLES

Patterns in vegetation composition and species coverage along the spatial chronosequence were explored with DCA and CCA. Both analyses showed the same general pattern, thus only CCA ordination diagrams are shown (Fig. 4). Samples from each study site form groups relatively distinct in the ordination space, although the high within-site variability determines zones of overlap between groups (Fig. 4a). Sites and vegetation assemblages arranged successively along the first ordination axis (Fig. 4), indicating a trend of progressive vegetation change along the chronosequence.

The eigenvalues for the DCA (0.482 and 0.152 for DCA 1 and DCA 2, respectively) were similar to those recorded for the CCA (0.364 and 0.162 for CCA 1 and CCA 2, respectively), suggesting that the explanatory variables included in the canonical analysis are adequate for explaining the variation in species composition and cover. In addition, the species-environmental correlations were relatively high for both analyses (Table 4), revealing a strong relationship between changes in the vegetation and the explanatory variables available. The first DCA and CCA axes are significantly and strongly correlated to site exposure dates (Fig. 4a, Table 4), indicating that the dominant pattern in community structure is the successional change associated with increasing time since site deglaciation. The second ordination axes are significantly correlated to surface topography, showing positive values for depressed surfaces and negative values for elevated surfaces (Fig. 4a, Table 4). Thus, microtopographic heterogeneity, such as elevated, depressed, and flat surface topography, can partially explain the within-site variability in vegetation structure. The canonical axes are also significantly correlated with percentage of bare rock surface, percentage of bare soil, and canopy coverage, reflecting the progressive occupation of the bare terrain by the vegetation as succession progresses.

TABLE 4

Correlation values (r) between vegetation ordination axes and explanatory variables. DCA (Detrended Correspondence Analysis); CCA (Canonical Correspondence Analysis). Species-environment correlations on DCA 1 and DCA2: r  =  0.86 and r  =  0.37, respectively; and on CCA 1 and CCA 2: r  =  0.89 and r  =  0.83, respectively. The statistical significance level of each explanatory variable was estimated in base of their partial effects (variability explained by the variable after accounting for the effects of other variables) as each variable is added to the model. All three categories of Topography were tested in conjunction for significance of their effect. Significance levels: **P < 0.01, *P < 0.05.

i1523-0430-43-1-35-t04.tif

Discussion

Primary succession on the bedrock outcrops of Glaciar Frías foreland follows a model of directional replacement of species (sensu Svoboda and Henry, 1987). An initial stage dominated by a crustose lichen is followed by a mid-successional stage characterized by a lichen-moss mat, whereas vascular plants diversified and increased in coverage during the late-successional stage (Fig. 4, Table 3).

The pioneer crustose lichen Placopsis perrugosa is a successful colonizer, with high growth rate and dispersal ability, and is frequently found dominating recently deglaciated terrains in Chile, New Zealand, and Antarctica (Orwin, 1970; Lindsay, 1978; Galloway, 1992). This lichen formed pure stands on the study rock outcrops during the first 50 years after deglaciation (Table 3). With increasing terrain age, P. perrugosa centers disintegrate probably due to limitations in nutrient transport from the periphery to the center of the thallus (Nash, 1996). The declining of P. perrugosa on the older study surfaces seems to be exclusively related to the species life-cycle, as no different lichens or mosses overgrow or develop in close contact to P. perrugosa competing for space.

Lichens are considered to be initiators of succession on rock surfaces because they significantly enhance rock weathering, derive inorganic nutrients from the rocks, and provide organic materials (Adamo and Violante, 2000). In addition, the presence of external cephalodia with cyanobacteria capable of fixing nitrogen in P. perrugosa significantly increases the nitrogen stock in the new substrates, where nitrogen is a limiting nutrient for plant colonization (Vitousek, 1994). However, we noted that rock surfaces exposed by P. perrugosa as the lichen centers degraded show little evidence of disaggregation and fragmentation, suggesting that the colonization of this lichen does not contributed much to rock weathering. In addition, P. perrugosa disappears from the rock surfaces before the widespread colonization by mid-successional species, indicating that there is not a direct interaction between this lichen and later colonizers. Therefore, the early colonization by P. perrugosa seems to contribute little to the establishment of later colonizers on rock outcrops in the study area. Our observations are consistent with studies questioning the role of pioneer crustose lichens in the primary succession process. For example, Longton (1992) and Kurina and Vitousek (2001) considered that crustose lichens are able to colonize bare surfaces early because of their ruderal life-cycle traits, but do not have relevant positive effects on later colonizers.

The development of a lichen-moss mat between 50 and 80 years after deglaciation marks the transition from the pioneer to the mid-successional stage. The species that dominated the mat (Racomitrium lanuginosum, Cladonia spp., and Stereocaulon spp.) are common pioneer colonizers during primary succession on glacier forelands, lava flows, and high mountain environments (Veblen and Ashton, 1979; Veblen et al., 1989; Vetaas, 1994; Hodkinson et al., 2003; Cutler et al., 2008). They are highly tolerant to stressful environmental conditions and have the ability to rapidly spread over intact rock surfaces as their rhizoids are able to penetrate into the superficial layers of rocks (Longton, 1992; Adamo and Violante, 2000). After about 110 years the lichen-moss mat forms an almost continuous, thick layer (ca. 15 cm) of organic material on rock surfaces at Glaciar Frías.

The expansion of the lichen-moss mat is followed by the high recruitment and increase in coverage of vascular plants (Tables 2 and 3). It is well known that cryptogamic mats contribute to soil formation by entrapping particulate material and retaining remnants of dead vegetation (Longton, 1992). The formation of a soil layer is highly relevant in rocky environments where growth of large-sized vascular plants is controlled by the presence of sites with adequate soil volume for root deployment (Burbanck and Phillips, 1983; Matthes-Sears and Larson, 1999). Cryptogams can also benefit vascular plants by ameliorating the physical and chemical environment, contributing nitrogen to the environment and entrapping plant seeds (Belnap et al., 2001; Breen and Lévesque, 2006). Therefore, the colonization of vascular plants observed during mid- and late-succession in the study area (Tables 2 and 3) likely has been facilitated by the earlier development of a cryptogamic carpet of mosses and fruticose lichens on the rock surfaces.

The colonization of vascular plants follows a physiognomic succession. Small, trailing shrubs and compact cushions (e.g. Senecio argyreus, Gaultheria pumila, G. caespitosa, Baccharis racemosa, Empetrum rubrum, Discaria nana, and Escallonia alpina) form a woody carpet by covering large portions of the rock surfaces by horizontal spreading and vegetative reproduction. As succession progresses, herbs, erect shrubs, and small Nothofagus dombeyi trees (up to 2 m high) colonize the rock outcrops, forming a community with many overlapping strata (Table 3). On deglaciated terrains and alpine treelines in the southern Patagonian Andes, the emergence, growth, and survival of N. antarctica and N. pumilio seedlings increase under the canopy of shrubs (e.g. Empetrum rubrum) or adult trees (Cuevas, 2000; Henríquez and Lusk, 2005). Veblen and Ashton (1979) also reported that the establishment of Nothofagus spp. on volcanic ashes needs the protection from strong winds given by prostrate shrubs. Although individuals of Nothofagus are sometimes initial colonizers on recently deglaciated surfaces (Lawrence and Lawrence, 1959; Villalba et al., 1990; Masiokas, 2008), in general they are isolated trees associated with safe sites, such as cracks protected from wind (Veblen et al., 1989). For example, Villalba et al. (1990) reported a solitary 29-year-old N. pumilio growing on moraine 7 at Glaciar Frías, indicating that no other specimen succeeded in establishing on this moraine during the subsequent three decades. Therefore, the protection provided by other plants can be of outmost importance for the regeneration of a Nothofagus stand under the severe environmental conditions prevailing in the Patagonian Andes.

Our study provides a detailed example of vegetation development on bedrock slopes following deglaciation, which can be compared to successional trajectories reported in the literature for unconsolidated glacial deposits in the Patagonian Andes. Unfortunately, few studies on unconsolidated deposits have included cryptogams, making difficult the comparison of the earlier stages of vegetation development on the different surfaces. Lichenological studies nearby Glaciar San Rafael, a wet-maritime area in the Patagonian Andes, showed that Placopsis spp. not only dominate boulders and rock surfaces but also consolidated gravel (Galloway, 1992). The dominance of Placopsis spp. has also been reported in other Patagonian glaciers (Winchester and Harrison, 2000). At Glaciar Casa Pangue, approximately 4 km to the west of Glaciar Frías (Fig. 1), cryptogams account for 57% of the total coverage on moraines 40 years after deglaciation (Veblen et al., 1989). The lichen Stereocaulon and the moss Racomitrium are common constituents of the community in the earlier stages of vegetation development in Glaciar Casa Pangue (Veblen et al., 1989). Therefore, there is a striking similarity in the vegetation communities developing on rock faces and glacial deposits during the pioneer and mid-stages of the primary succession.

The woody carpet of prostrate shrubs observed on Glaciar Frías outcrops is a common stage of vegetation succession on areas exposed by glacier retreat or affected by volcanism in the Patagonian Andes (Heusser, 1964; Veblen and Ashton, 1979; Veblen et al., 1989; and personal observations). On unconsolidated glacial deposits, the shrubby vegetation is usually replaced by Nothofagus-dominated forests within 75 years since glacier retreat (Heusser, 1964; Villalba et al., 1990). In contrast, we recorded a sparse coverage of N. dombeyi saplings in the rock outcrops exposed for more than 140 years (Table 3). This indicates that vegetation development is greatly delayed on rock outcrops compared to unconsolidated deposits. It is known that the slower community establishment on bare rock outcrops is related to the long time required for the formation of a ground vegetation cover and an organic matter layer (Asselin et al., 2006). These observations are consistent with our results indicating that once the lichen-moss mat develops, a large diversity of vascular plants rapidly colonized the rock surfaces. Indeed, the coverage of the vascular plants increased almost fivefold between sites 4 to 5, i.e. in a period of approximately 35 years (Fig. 3, Table 2). In summary, vegetation development requires at least 100 years longer on bedrock outcrops than on unconsolidated glacial deposits and is closely related to the time required for the formation of a cryptogamic carpet.

Acknowledgments

This work was funded by the Argentinean Agency for the Promotion of Science (grant PICTR02-186 and PICT32003), the Argentinean Council of Research and Technology (CONICET), and by the Inter-American Institute for Global Change Research (IAI) CRN II # 2047, which is supported by the U.S. National Science Foundation (grant GEO-0452325). We thank T. Ahti (Helsinki University, Finland) and G. Calabrese (University of Río Negro, Argentina) for help identifying lichen and moss species, respectively. The authors thank two anonymous reviewers for constructive criticism of the original manuscript.

References Cited

1.

P. Adamo and P. Violante . 2000. Weathering of rocks and neogenesis of minerals associated with lichen activity. Applied Clay Sciences 16:229–256. Google Scholar

2.

A. C. Archer, M. J. A. Simpson, and B. H. MacMillan . 1973. Soils and vegetation of the lateral moraine at Malte Brun, Mount Cook region, New Zealand. New Zealand Journal of Botany 11:23–48. Google Scholar

3.

J. J. Armesto, I. Casassa, and O. Dollenz . 1992. Age structure and dynamics of Patagonian beech forests in Torres del Paine National Park, Chile. Vegetatio 98:13–22. Google Scholar

4.

D. H. Ashton and G. M. Moore . 1978. Vegetation of Pleistocene block streams and block fields in Victoria: a successional interpretation. Australian Journal of Ecology 3:43–56. Google Scholar

5.

H. Asselin, A. Belleau, and Y. Bergeron . 2006. Factors responsible for the co-occurrence of forested and unforested rock outcrops in the boreal forest. Landscape Ecology 21:271–280. Google Scholar

6.

V. Barros, V. Cordon, C. Moyano, R. Mendez, J. Forquera, and O. Pizzio . 1983. Cartas de Precipitación de la Zona Oeste de las Provincias de Río Negro y Neuquén. Cinco Saltos, Argentina Facultad de Ciencias Agrarias, Universidad Nacional del Comahue. pp.  Google Scholar

7.

J. Belnap, R. Prasse, and K. T. Harper . 2001. Influence of biological soil crusts on soil environments and vascular plants. In J. Belnap and O. L. Lange . (eds.). Biological Soil Crusts: Structure, Function, and Management. Berlin-Heidelberg Springer-Verlag. 281–300. Google Scholar

8.

K. Breen and E. Lévesque . 2006. Proglacial succession of biological soil crusts and vascular plants: biotic interactions in the High Arctic. Canadian Journal of Botany 84:1714–1731. Google Scholar

9.

R. K. Brummitt and C. E. Powell . 1992. Authors of Plants Names. Kew Royal Botanical Garden. pp.  Google Scholar

10.

M. P. Burbanck and D. L. Phillips . 1983. Evidence of plant succession on granite outcrops of the Georgia piedmont. The American Midland Naturalist 109:94–104. Google Scholar

11.

J. G. Cuevas 2000. Tree recruitment at the Nothofagus pumilio alpine timberline in Tierra del Fuego, Chile. Journal of Ecology 88:840–855. Google Scholar

12.

N. A. Cutler, L. R. Belyea, and A. J. Dugmore . 2008. The spatiotemporal dynamics of a primary succession. Journal of Ecology 96:231–246. Google Scholar

13.

F. S. Chapin III, L. R. Walker, C. L. Fastie, and L. C. Sharman . 1994. Mechanisms of primary succession following deglaciation at Glacier Bay, Alaska. Ecological Monographs 64:149–175. Google Scholar

14.

A. De Agostini 1945. Andes Patagónicos. Buenos Aires Guillermo Kraft Ltda. pp.  Google Scholar

15.

R. del Moral, J. H. Titus, and A. M. Cook . 1995. Early primary succession on Mount St. Helens, Washington, USA. Journal of Vegetation Science 6:107–120. Google Scholar

16.

O. Dollenz 1991. Sucesión vegetal en el sistema morrenico del Glaciar Dickson, Magallanes, Chile. Anales del Instituto de la Patagonia Serie Ciencias Naturales 20:49–60. Google Scholar

17.

C. Ezcurra and C. Brion . 2005. Plantas del Nahuel Huapi: Catálogo de la Flora Vascular del Parque Nacional Nahuel Huapi, Argentina. San Carlos de Bariloche, Argentina Universidad Nacional del Comahue. pp.  Google Scholar

18.

F. Fonck 1896. Viajes del Fray Francisco Menéndez a la Cordillera. Valparaiso, Chile Niemeyer. pp.  Google Scholar

19.

B. L. Foster and D. Tilman . 2000. Dynamic and static views of succession: testing the descriptive power of the chronosequence approach. Plant Ecology 146:1–10. Google Scholar

20.

D. J. Galloway 1992. Lichens of Laguna San Rafael, Parque Nacional “Laguna San Rafael”, southern Chile: indicators of environmental change. Global Ecology and Biogeography Letters 2:37–45. Google Scholar

21.

J. M. Henríquez 2004. Influencia de los defecaderos de camélidos sobre el desarrollo vegetal y riqueza de especies en morenas glaciales, Tierra del Fuego. Revista Chilena de Historia Natural 77:501–508. Google Scholar

22.

J. M. Henríquez and C. H. Lusk . 2005. Facilitation of Nothofagus antarctica (Fagacea) seedlings by the prostrate shrub Empetrum rubrum (Empetraceae) on glacial moraines in Patagonia. Austral Ecology 30:877–882. Google Scholar

23.

C. J. Heusser 1960. Late-Pleistocene environments of the Laguna de San Rafael area, Chile. Geographical Review 50:555–577. Google Scholar

24.

C. J. Heusser 1964. Some pollen profiles from Laguna San Rafael area, Chile. In L. M. Cranwell (ed.). Ancient Pacific Floras. Honolulu, U.S.A University of Hawaii Press. 95–114. Google Scholar

25.

I. D. Hodkinson, S. J. Coulson, and N. R. Webb . 2003. Community assembly along proglacial chronosequences in the High Arctic: vegetation and soil development in north-west Svalbard. Journal of Ecology 91:651–663. Google Scholar

26.

R. H. G. Jongman, C. J. F. ter Braak, and O. F. R. Van Tongeren . 1995. Data Analysis in Community and Landscape Ecology. Cambridge, U.K Cambridge University Press. pp.  Google Scholar

27.

C. Körner 2005. The green cover of mountains in a changing environment. In U. M. Huber, H. K. M. Bugmann, and M. A. Reasoner . (eds.). Global Change and Mountain Regions, an Overview of Current Knowledge. Dordrecht, The Netherlands Springer. 367–375. Google Scholar

28.

L. M. Kurina and P. M. Vitousek . 2001. Nitrogen fixation rates of Stereocaulon vulcani on young Hawaiian lava flows. Biogeochemistry 55:179–194. Google Scholar

29.

P. J. D. Lambshead, H. M. Platt, and K. M. Shaw . 1983. The detection of differences among assemblages of marine benthic species based on an assessment of dominance and diversity. Journal of Natural History 17:859–874. Google Scholar

30.

D. B. Lawrence and E. G. Lawrence . 1959. Recent Glacier Variations in Southern South America. New York American Geographical Society. pp.  Google Scholar

31.

J. Leps and P. Šmilauer . 1999. Multivariate Analysis of Ecological Data. Ceske Budejovice Faculty of Biological Sciences, University of South Bohemia. pp.  Google Scholar

32.

D. C. Lindsay 1978. The role of lichens in Antarctic ecosystems. The Bryologist 81:268–276. Google Scholar

33.

R. E. Longton 1992. The role of bryophytes and lichens in terrestrial ecosystems. In J. W. Bates and A. M. Farmer . (eds.). Bryophytes and Lichens in a Changing Environment. Oxford Oxford University Press. 32–75. Google Scholar

34.

B. H. Luckman and R. Villalba . 2001. Assessing the synchroneity of glacier fluctuations in the western Cordillera of the Americas during the last millennium. In V. Makgraf (ed.). Interhemispheric Climate Linkages. San Diego Academic Press. 119–140. Google Scholar

35.

A. E. Magurran 1988. Ecological Diversity and its Measurements. Princeton Princeton University Press. pp.  Google Scholar

36.

M. Masiokas 2008. Climate and glacier variability during past centuries in the north and south Patagonian Andes of Argentina. Ph.D. thesis. Faculty of Graduate Studies, The University of Western Ontario, London, Ontario, Canada. pp.  Google Scholar

37.

M. Masiokas, B. H. Luckman, R. Villalba, A. Ripalta, and J. Rabassa . 2010. Little Ice Age fluctuations of Glaciar Río Manso in the north Patagonian Andes of Argentina. Quaternary Research 73:96–106. Google Scholar

38.

U. Matthes-Sears and D. W. Larson . 1999. Limitations to seedling growth and survival by the quantity and quality of rooting space: implications for the establishment of Thuja occidentalis on cliff faces. International Journal of Plant Sciences 160:122–128. Google Scholar

39.

U. Matthes-Sears and D. W. Larson . 2006. Microsite and climatic controls of tree population dynamics: an 18-year study on cliffs. Journal of Ecology 94:402–414. Google Scholar

40.

J. A. Matthews 1992. The Ecology of Recently Deglaciated Terrain. A Geological Approach to Glacier Forelands and Primary Succession. Cambridge, U.K Cambridge University Press. pp.  Google Scholar

41.

J. A. Matthews 1999. Disturbance regimes and ecosystem response on recently-deglaciated substrates. In L. R. Walker (ed.). Ecosystems of Disturbed Ground. Amsterdam Elsevier. 17–37. Google Scholar

42.

J. A. Matthews and R. J. Whittaker . 1987. Vegetation succession on the Storbreen Glacier Foreland, Jotunheimen, Norway: a review. Arctic and Alpine Research 19:385–395. Google Scholar

43.

T. H. Nash III 1996. Photosynthesis, respiration, productivity and growth. In T. H. Nash III (ed.). Lichen Biology. Cambridge, U.K Cambridge University Press. 88–120. Google Scholar

44.

B. M. Opazo Medina, K. Torres Ribeiro, and F. Rubio Scarano . 2006. Plant-plant and plant-topography interactions on a rock outcrop at high altitude in southeastern Brazil. Biotropica 38:27–34. Google Scholar

45.

J. F. Orwin 1970. Lichen succession on recently deposited rock surfaces. New Zealand Journal of Botany 8:452–477. Google Scholar

46.

J. F. Orwin 1972. The effect of environment on assemblages of lichens growing on rock surfaces. New Zealand Journal of Botany 10:37–47. Google Scholar

47.

F. Paul, A. Kääb, and W. Haeberli . 2007. Recent glacier changes in the Alps observed by satellite: consequences for future monitoring strategies. Global and Planetary Change 56:111–122. Google Scholar

48.

M. S. Pelto 2009. Forecasting temperate alpine glacier survival from accumulation zone observations. The Cryosphere Discussions 3:323–350. Google Scholar

49.

S. T. A. Pickett 1989. Space-for-time substitution as an alternative to long-term studies. In G. E. Likens (ed.). Long-Term Studies in Ecology. New York Springer. 110–135. Google Scholar

50.

V. E. Pisano 1978. Establecimientos de Nothofagus betuloides (Mirb.) Blume (Coigue de Magallanes) en un valle en proceso de deglaciación. Anales del Instituto de la Patagonia, Serie Ciencias Naturales 9:107–128. Google Scholar

51.

J. Rabassa, S. Rubulis, and J. Suarez . 1978. Los glaciares del Monte Tronador, Parque Nacional Nahuel Huapi, Río Negro, Argentina. Anales de Parques Nacionales 14:259–295. Google Scholar

52.

J. Rabassa, S. Rubulis, and J. Suarez . 1979. Rate of formation and sedimentology of (1976–1978) push-moraines, Frías Glacier, Mount Tronador (41 10′S; 71 53′W), Argentina. In C. H. Schlucher (ed.). Moraines and Varves. Rotterdam Balkema. 65–80. Google Scholar

53.

J. Rabassa, S. Rubulis, and J. Suarez . 1981. Moraine in-transit as parent material for soil development and the growth of Valdivian Rain Forest on moving ice: Casa Pangue Glacier, Mount Tronador (Lat. 41°10′S), Chile. Annals of Glaciology 2:97–102. Google Scholar

54.

A. Rivera and G. Casassa . 2004. Ice elevation, areal, and frontal changes of glaciers from National Park Torres del Paine, southern Patagonia Icefield. Arctic, Antarctic, and Alpine Research 36:379–389. Google Scholar

55.

C. Sarthou, C. Kounda-Kiki, A. Vaculik, P. Mora, and J-F. Ponge . 2009. Successional patterns on tropical inselbergs: a case study on the Nouragues inselberg (French Guiana). Flora 204:396–407. Google Scholar

56.

D. J. Shure and H. L. Ragsdale . 1977. Patterns of primary succession on granite outcrop surfaces. Ecology 58:993–1006. Google Scholar

57.

P. Sommerville, A. F. Mark, and J. B. Wilson . 1982. Plant succession on moraines of the upper Dart Valley, southern South Island, New Zealand. New Zealand Journal of Botany 20:227–244. Google Scholar

58.

H. Steffen 1909. Viajes de Esploracion i Estudio en la Patagonia Occidental: 1892–1902. Santiago de Chile Imprenta Cervantes. pp.  Google Scholar

59.

J. Svoboda and G. H. R. Henry . 1987. Succession in marginal Arctic environments. Arctic and Alpine Research 19:373–384. Google Scholar

60.

G. E. Uno and S. L. Collins . 1987. Primary succession on granite outcrops in southwestern Oklahoma. Bulletin of the Torrey Botanical Club 114:387–392. Google Scholar

61.

A. T. Veblen and D. H. Ashton . 1979. Successional pattern above timberline in south-central Chile. Vegetatio 40:39–47. Google Scholar

62.

T. T. Veblen, D. H. Ashton, S. Rubulis, D. C. Lorenz, and M. Cortes . 1989. Nothofagus stand development on in-transit moraines, Casa Pangue Glacier, Chile. Arctic and Alpine Research 21:144–155. Google Scholar

63.

O. R. Vetaas 1994. Primary succession of plant assemblages on a glacier foreland—Bodalsbreen, southern Norway. Journal of Biogeography 21:297–308. Google Scholar

64.

R. Villalba, J. C. Leiva, S. Rubulis, J. Suarez, and L. Lenzano . 1990. Climate, tree-ring, and glacial fluctuations in the Río Frías Valley, Río Negro, Argentina. Arctic, Antarctic, and Alpine Research 22:215–232. Google Scholar

65.

P. M. Vitousek 1994. Potential nitrogen fixation during primary succession in Hawai'i Volcanoes National Park. Biotropica 26:234–240. Google Scholar

66.

L. R. Walker and F. S. Chapin III . 1987. Interactions among processes controlling successional change. Oikos 50:131–135. Google Scholar

67.

L. R. Walker, D. A. Wardle, R. D. Bardgett, and B. D. Clarkson . 2010. The use of chronosequences in studies of ecological succession and soil development. Journal of Ecology doi:10.1111/j.1365-2745.2010.01664.x. Google Scholar

68.

P. Wardle 1980. Primary succession in Westland National Park and its vicinity, New Zealand. New Zealand Journal of Botany 18:221–232. Google Scholar

69.

V. Winchester and S. Harrison . 2000. Dendrochronology and lichenometry: colonization, growth rates and dating of geomorphological events on the east side of the North Patagonian Icefield, Chile. Geomorphology 34:181–194. Google Scholar

70.

S. K. Wiser, R. K. Peet, and P. S. White . 1996. High-elevation rock outcrop vegetation of the southern Appalachian Mountains. Journal of Vegetation Science 7:703–722. Google Scholar

71.

I. O. Zuloaga and O. Morrone . 1999a. Catálogo de las Plantas Vasculares de Argentina I. St. Louis, Missouri Missouri Botanical Garden. pp.  Google Scholar

72.

I. O. Zuloaga and O. Morrone . 1999b. Catálogo de las Plantas Vasculares de Argentina II. St. Louis, Missouri Missouri Botanical Garden. pp.  Google Scholar
Irene A. Garibotti, Clara I. Pissolito, and Ricardo Villalba "Vegetation Development on Deglaciated Rock Outcrops from Glaciar Frías, Argentina," Arctic, Antarctic, and Alpine Research 43(1), 35-45, (1 February 2011). https://doi.org/10.1657/1938-4246-43.1.35
Accepted: 1 July 2010; Published: 1 February 2011
JOURNAL ARTICLE
11 PAGES


SHARE
ARTICLE IMPACT
Back to Top