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Vegetation History and Archaeobotany

, Volume 19, Issue 3, pp 191–206 | Cite as

High-resolution studies on vegetation succession, hydrological variations, anthropogenic impact and genesis of a subrecent lake in southern Ecuador

  • Corinna BrunschönEmail author
  • Torsten Haberzettl
  • Hermann Behling
Open Access
Original Article

Abstract

A lake sediment record from Laguna Campana at 2,488 m a.s.l. in the eastern Ecuadorian Andes allows the reconstruction of local environmental conditions over the past ~500 years. A high-resolution multi-proxy approach using pollen, spore, charcoal and XRF analyses provides information about lake genesis, hydrological variations and the development of the surrounding vegetation. Results suggest that Laguna Campana originated from a landslide, which are naturally common and anthropogenically promoted in the study area. Human activities, e.g. deforestation or slash and burn cultivation, impacted the local vegetation development and biodiversity during the recorded period. After a first dense layer of pioneer grasses developed on open soil around the small lake, successional stages of secondary upper mountain rainforest forest mainly composed of Alnus and Weinmannia were observed. The record shows no signs of dense forest regeneration but rather open vegetation with trees and a grassy understory. Especially since ca. a.d. 1980, the proportion of forest in the area was reduced, most probably by fire use for pastures, cultivation and wood extraction. Hydrological variability was derived from differences in minerogenic input and variations in Botryococcus braunii and Sphagnum occurrence. After wettest conditions at the study site, probably triggering the landslide, humid conditions persisted until a time of drier conditions between a.d. 1900 and 1960. A subsequent return to wetter conditions was observed over the last decades. XRF analyses suggest an increase in deposition of atmospherically derived lead since the formation of the lake.

Keywords

Multi-proxy Pollen Vegetation history Anthropogenic impact Lead Hydrological variability Ecuadorian Andes 

Introduction

Tropical mountain regions, as occur in the eastern Andes of Ecuador, are emphasized as holding the world’s most significant biodiversity hotspots (Barthlott et al. 2005). Different environmental conditions are responsible for this phenomenon. Among the triggers of biodiversity, for example the complex topography and highly varied climatic conditions can be specified for the Andean region. Additionally, the uplift of mountain chains causing an extensive evolutionary radiation should be considered in terms of species richness and biodiversity levels (Richter 2008). Hence, tropical mountain ecosystems and their origin play an important role in biodiversity research. However, palaeoecological records in mountain forests of the Andean region are thinly scattered not least because of the steep slopes and scarcity of natural archives (Bush et al. 2007). The first palynological studies in the eastern Ecuadorian Andes focusing on the Podocarpus National Park (PNP) and its megadiverse mountain ecosystems have been carried out recently (Beck et al. 2008a). Several palaeoecological analyses of sediment cores at high elevations up to 3,300 m a.s.l. were used to begin a comprehensive reconstruction of late Quaternary vegetation of the PNP (Brunschön and Behling 2009; Niemann and Behling 2008a, b; Niemann and Behling 2009, 2010; Niemann et al. 2009).

Within the South American countries Ecuador currently suffers from the highest deforestation rate of 198,000 ha year−1 (FAO 2006). Already during pre-Columbian times a long-lasting deforestation in the mountain regions had contributed to the reduction of forest areas (Wunder 2000). Early human settlements were accompanied by land use for cultivation and pastures, converting natural landscapes into man-made environments on a large scale. During the most recent times agricultural colonization due to increasing population is further amplified by infrastructure improvements (Pohle 2008). Extensive road construction and other anthropogenic factors additionally promote wide-spread landslides in the Ecuadorian Andes, which are also naturally triggered, for example by unstable slopes and perhumid environmental conditions (Lozano et al. 2005). The landslides are assumed to play an important role in maintaining species diversity in tropical mountain forests (Guariguata 1990; Kessler 1999).

This study focuses on environmental and vegetation dynamics of mountain ecosystems in the area of the Podocarpus National Park. High-resolution multi-proxy palaeoecological analyses of the Laguna Campana sediment record (Fig. 1) are used to provide detailed insights into palaeoenvironmental variations. This will allow the identification of possible past human influences and their potential impacts on local vegetation and biodiversity.
Fig. 1

Map showing a the location of Ecuador in South America, b the Andes (shaded area) and the limits of the Podocarpus National Park and c a detailed sketch of the research area between the cities of Loja and Zamora. The study site Laguna Campana is located at 2488 m a.s.l. west of the northern Podocarpus National Park area

Study site

Location

Laguna Campana (04°01′28″ S, 79°10′40″ W) is located on the western slope of the Cordillera Real, an eastern Andean range of Southern Ecuador at an elevation of 2,488 m a.s.l. (Fig. 1). Nearby crests reach elevations of up to ~3,100 m. The study area is about 5 km southeast of the city of Loja (2,100 m a.s.l., Fig. 1) and 2 km west of the Podocarpus National Park (PNP), which is located between the provinces of Loja and Zamora-Chinchipe. The small village of Zamora Huayco Alto is situated west of Laguna Campana about 300 m downhill. Observations of surrounding geomorphologic structures suggest that Laguna Campana was probably formed by a landslide the age of which is, hitherto, unknown. Nowadays, the small lake neither has an inflow nor an outflow. It has a maximum water depth of 1.5 m and covers an area of about 1,500 m2.

Geomorphology and geology

The so called Girón-Cuenca and Huancabamba Andean depression region in the eastern Andean range of southern Ecuador and northern Peru (2–6° S) is characterised by low elevations not exceeding 4,000 m a.s.l. (Richter and Moreira-Muñoz 2005). Volcanoes as well as glaciers are absent (Schubert and Clapperton 1990). Hence, volcanic contributions to the sediments of Laguna Campana are negligible. The area of the Andean depression, where the study site is located, consists of a complicated topography as a junction of mountain ranges culminates in the so called “Nudo de Loja”, from which Inter-Andean Sierras stretch in different directions dissected by valleys and basins (Beck et al. 2008b). The eastern Andean Cordillera is mainly made up of Paleozoic metamorphic rocks (Baldock 1982). Rocks around Loja consist of mica schists, gneisses and granites. The basin margins contain conglomerates of metamorphic debris and argillaceous sandstone in the Miocene layers, which promote landslides of water saturated soils (Sauer 1971). Landslides in the tropical mountain forests of Ecuador are mostly shallow soil removals. Often only O-horizons and upper parts of the A-horizons are displaced further downslope (Bussmann et al. 2008). Geomorphologic evidence for landslides can be observed all around the study site including Laguna Campana.

Climate

The climate of Ecuador including the study area is dominated by the tropical trade wind regime characterised by strong easterlies bringing moist air masses from the Amazon basin (Beck et al. 2008b). The Cordillera Real acts as a climatic divide separating moist conditions on the Amazon exposed eastern side from the (semi-) arid climate on the west (Emck 2007). East of the Cordillera, precipitation and humidity rise continuously to the crest regions. The western escarpment and the Inter-Andean zone belong to the greater lee of the Cordillera Real, where arid conditions start immediately behind the climate divide. Rainfall of 6,000 mm a−1 at 3,100 m a.s.l. contrasts with the Inter-Andean basin, which receives generally less than 1,000 mm a−1 (Emck 2007; Bendix et al. 2008a). As Laguna Campana is located on the western slopes of Cordillera Real it faces the dry Inter-Andean basin (Fig. 1). Rainfall variability reveals a diurnal and seasonal pattern in the study area. Variations caused by ENSO (El Niño-Southern Oscillation) do not have an influence as the region is sheltered from Pacific air masses by the mountain ranges (Bendix et al. 2008b).

Temperature varies according to the time of day and season. The austral winter is the wettest and coldest period of the year (Bendix et al. 2008a). Laguna Campana is situated between the so called “tierras templadas and frescas” (temperate and cool land), where soil temperature of ca. 15°C and 9–12 humid months are observed. Measurements at Loja (2,160 m a.s.l., 2.5 km from Laguna Campana) indicate a mean annual precipitation of 922–947 mm and a mean annual temperature of 15.5°C (Richter and Moreira-Muñoz 2005; Günter et al. 2008).

Modern vegetation

The potential vegetation in the PNP area was described by Homeier et al. (2008) and citations therein (e.g. Lozano 2002; Aguirre et al. 2003; Richter 2003). Accordingly, five of the potential natural vegetation types describe the area surrounding Laguna Campana best: lower and upper mountain rainforest, interandean semideciduous forest, subpáramo and páramo. The study site and large areas in the provinces of Loja and Zamora-Chinchipe surrounding the PNP are degraded. The natural vegetation has been modified by anthropogenic activities such as road construction, deforestation, fire use and pastures.

Lower mountain rainforest (LMF) with a canopy height of 30 m is found at ca. 1,300–2,100 m a.s.l. on the eastern escarpment of the Cordillera Real. Characteristic species are among others Cyathea caracasana, Morus insignis, Piper sp., Mikania sp. and Heliocarpus americanus.

Laguna Campana is located in the potential vegetation type of upper mountain rainforest (UMF) between ca. 2,400–2,700 m a.s.l. on the western escarpment above Loja. The canopy attains heights of up to 20 m. Some of the main key species are Hedyosmum racemosum, Weinmannia sp., Myrica pubescens, Myrsine andina, Prumnopitys montana, Clusia sp. and Cedrela montana. It was observed in the field that the vegetation in the area frequently burned, promoting sparse shrubland dominated by burnt Puya plants on open soils. Pinus is found in the surroundings. The UMF on the eastern escarpment (ca. 2,100–2,700 m a.s.l.) varies in species composition and reaches a canopy height of up to 25 m. Some key species which differ from those of the western slope are, e.g. Ilex rimbachii, Purdiaea nutans, Macrocarpaea revoluta, Podocarpus oleifolius and Dioicodendron dioicum.

At ca. 2,700–3,100 m a.s.l. on the eastern and western escarpment subpáramo vegetation is present, including a subtype of elfin forest forming the upper forest line ecotone. Canopy heights are 6–8 m and for the subpáramo a little less. Characteristic species are, e.g. Clethra ovalifolia, Gaultheria reticulata, Gaiadendron punctatum, Graffenrieda harlingii and Hesperomeles ferruginea.

Páramo (including shrub and herb páramo) is found above the upper forest line at ca. 3,100–3,600 m elevation. Páramo vegetation is characterised by a maximum height of 2 m. Some key species are Puya eryngioides, Rhynchospora vulcani, Chusquea neurophylla, Monnina arbuscula and Valeriana microphylla.

South-west of the study site in the basin at ca. 1,400–2,400 m a.s.l. interandean semideciduous forest (SDF) is found. The canopy height reaches 15 m, occasionally about 20 m. Some indicator species are Ceiba insignis, Croton wagneri, Acacia macracantha, Anadenanthera colubrine and Dodonaea viscosa.

Materials and methods

For sediment sampling in the centre of Laguna Campana two different corers were used from a fixed rubber dinghy. The upper 20 cm of unconsolidated, water saturated sediment were recovered using an UWITEC Corer (http://www.uwitec.at/). Every 2 cm subsamples of sediment were taken in the field. Subsequently, a core of 82 cm was taken with a Livingstone piston corer from 15 to 97 cm depth of sediment. This sediment section was recovered in an aluminum tube and stored under dark and cold (4°C) conditions until processing.

Subsamples for pollen analysis were taken at 2 cm intervals except for a 1 cm sampling interval in the transition zone between the two different core sections (14–19 cm). In total 52 subsamples were processed applying standard pollen analytical methods (Fægri and Iversen 1989). Exotic Lycopodium spores were added as a marker to each subsample for calculation of concentrations. The pollen sum of a minimum of 300 pollen grains includes pollen of trees, shrubs and herbs as well as unknown and indeterminate pollen types. Based on this sum percentage data of each pollen type were calculated. Spores and algae (e.g. Botryococcus braunii) were also counted and quantified as percentages of the pollen sum. Charcoal particles (5–150 μm) were counted on each pollen slide and presented as percentage data relative to the pollen sum. Additional concentration data were calculated for Botryococcus braunii, the pollen sum and charcoal particles.

Pollen and spore identification was mainly based on the reference collection kept at the University of Göttingen, which contains ~3,000 Neotropical (Behling 1993) and approximately 300 Ecuadorian pollen and spore types, and a published pollen reference from Colombia (Hooghiemstra 1984). Identified pollen types were classified in ecological groups referring to described potential natural vegetation types of the area by Homeier et al. (2008) and available data on plant ecology and distribution (Bussmann 2001; Lozano 2002; Marchant et al. 2002; Richter and Moreira-Muñoz 2005; Homeier and Werner 2008). Indicators of cultivation and plantation as well as unknown pollen types were grouped separately.

For pollen data calculation and illustration the software TILIA and TILIAGRAPH (Grimm 1991, 2004) was used. Classification of zones was based on a constrained clusters analysis of all pollen taxa performed by CONISS (Grimm 1987) and on changing abundances of the most important pollen taxa. A further subdivision of one zone was supported by significant variations in XRF data.

Non-destructive XRF-scanning was done using an ITRAX core scanner (Croudace et al. 2005; St-Onge et al. 2007) with a 1 mm step size. Element count rates are given in element peak areas (pa, element integral). The X-ray radiography was obtained with the same device. Subsequently, a principle component analysis (PCA) was done using log transformed values of all elements showing a mean of more than 100 pa (Fig. 2). Values of PC1 were multiplied by -1 in order to facilitate the comparison with the curves contributing to this PC.
Fig. 2

Principle Component Analysis (PCA) of all elements showing an average above 100 pa (peak area)

PC1 reduces all the allochthonous minerogenic input parameters hitherto frequently used in other studies, such as the conservative lithogenic metal Ti (Shotyk et al. 2001; Haberzettl et al. 2005, 2006, 2007, 2008; Niemann et al. 2009) or Rb (Guyard et al. 2007), to one proxy. Hence, increases in that proxy represent an increase in runoff or eolian supply. Alternatively, PC1 mirrors the plant coverage in the catchment area. Low coverage especially immediately after a landslide would result in intensified erosion and therefore increased minerogenic input to the lake.

The incoherent/coherent (inc/coh) ratio may be used as an estimate of sediment organic content (Guyard et al. 2007; Rolland et al. 2008). This explains the opposite pattern of this ratio to PC1. If the minerogenic content decreases the relative proportion of organic material rises and vice versa.

Due to its stability and high resistance to chemical weathering, Ti is widely used in geochemical studies as a conservative metal, against which relative enrichments and depletions of more mobile major and trace elements like Fe, Pb or Cu may be compared (Shotyk et al. 2001). The Fe/Ti ratio is a measure of redox processes. If the ratio is constant the Fe content resembles the minerogenic input and an influence of redox processes on this element is rather unlikely. For iron the critical Eh for reduction of Fe3+ compounds to more soluble Fe2+ compounds is 100 mV (Sigg and Stumm 1996). Therefore, if the redox potential drops to values below 100 mV, Fe/Ti ratios will decrease. If the migrating Fe ions oxidize again they will stop migrating and increase the Fe/Ti ratio.

Pb is a measure of the lead content of the sediment relative to sediments deposited above or below. In contrast, the Pb/Ti and Cu/Ti ratio reflect the Pb and Cu input relative to the minerogenic input. This means that if the ratios are not constant the changes are either caused by variations in atmospheric deposition independent of eolian and fluvial input, or by displacement of ions within the profile.

For AMS radiocarbon dating three subsamples, one bulk sample from the bottom of the record and two small leaves further up in the core, were submitted to the University of Erlangen-Nürnberg, Germany and to the Poznan Radiocarbon Laboratory, Poland (Table 1). For calibration of the 14C dates the online program CALIB 5.0.2 (Stuiver and Reimer 1993) with the Southern Hemisphere calibration set shcal04 (McCormac et al. 2004) was used. The calibrated dates given reflect the median ages of the 2σ distribution, as a single robust estimate, such as the weighted average or median, should be used (Telford et al. 2004).
Table 1

List of radiocarbon dates and calibrated ages from Laguna Campana

Lab. code

Depth (cm)

Sample description

14C Age (b.p.)

Calibrated (a.d.) (median)

2-σ range (a.d.)

Poz-24273

62

Leaf

101 ± 27

1880

1700–1955

Erl-13235

73

Leaf

490 ± 43

1450

1405–1615

Erl-11389

97

Bulk

456 ± 36

1470

1425–1620

Results

Lithology

Macroscopic inspections revealed that the sediment mainly consists of homogenous black organic rich material. The lower part between 97 and 80 cm showed the highest sediment density. The water content increases gradually to the top of the core and the upper 15 cm of the sediment are explicitly unconsolidated and water saturated. This trend is confirmed by the X-ray image (Fig. 3). At the bottom of the record the X-ray image reveals two zones (around 95 and 83 cm depth) of disturbed sediment separated by the most dense part of the record (93–87 cm depth). In the middle part of the core material of low density is found (Fig. 3). Unfortunately, no X-ray information is available from the upper 15 cm as they had already been subsampled in the field.
Fig. 3

Profiles of Principle Component 1 (PC1), XRF-scanning elemental analyses and radiograph of the sediment record from Laguna Campana. Values of PC1 were multiplied by -1 in order to facilitate the comparison with the curves contributing to this PC. XRF-data are plotted as ratios and Pb as element peak area (pa). Data for PC1 are smoothed with a 3-point moving average, for Pb with a 21-point moving average and for Pb/Ti as well as Cu/Ti with an 11-point moving average

Chronology and age-depth modelling

Radiocarbon dates show an age of a.d. 1880 +75/−180 at 62 cm depth of sediment and a basal age of the sediment core at 97 cm of a.d. 1470 +150/−45 (Table 1). A further radiocarbon date at 73 cm depth of sediment indicates an age of a.d. 1450 +165/−45, which is in the same range as the basal date. Both ages, at 73 and 97 cm, show a distinct offset to the upper age in the record.

As the formation of the lake is supposed to be associated with a landslide, which probably caused bare surfaces in the catchment area to be prone to erosion, an increased sedimentation rate as well as intense reworking seems to be plausible after soil movement. This might also have led to the inclusion of reworked organic compounds in the dating for the lowermost ages. The potential reworking is supported by PC1, which after a pronounced decrease from the bottom of the record up to 75 cm shows a final small increase from 75 to 72 cm. As PC1 represents allochthonous minerogenic input it is also possible that allochthonous organic components might have been transported to the lake. Hence, these two dates yield only a terminus post quem of ~a.d. 1470 for the base of the record and were excluded from the age-depth model (Fig. 4). Therefore, only one radiocarbon age can be used and other time markers have to be included generating an appropriate age-depth model for the record above the uppermost rejected date, i.e. 72 cm. The occurrence of Pinus pollen can be used as time marker, as this European tree species was introduced to Ecuador around the turn of the twentieth century (Neill 1999). Therefore, an extra scan of pollen slides exclusively for Pinus pollen starting at the bottom of the record was done in addition to the pollen count. The first Pinus pollen was observed at 55 cm (not included in the pollen sum and thus not displayed in the pollen diagram), which consequently indicates an age of a.d. 1900 for this sediment depth.
Fig. 4

Age-depth model for the Laguna Campana lake sediment record. The shaded area represents a section potentially yielding ages that are too old, possibly related to the initial landslide forming the lake and subsequent bare soil areas in the catchment

The age-depth model for the upper part of the record was built using the sediment/water interface as a time marker for the year of coring, i.e. 2007, the first occurrence of Pinus and the one accepted radiocarbon age at 62 cm. Linear interpolation between the sediment/water interface and the uppermost radiocarbon date does not account for the fact that potentially the top of the uppermost part of the record might be less affected by compaction. Hence, a second order polynomial function (y = −0.00129x 2 + 4.53182x − 3893.18714) was chosen (Fig. 4). The mean sedimentation rate for the upper part of the core is 4.97 mm a−1 or ~2 a cm−1.

XRF and pollen data

The PCA of the XRF data shows that PC1 is mainly formed by K, Ti, Fe, Rb, Zr and Cu (Fig. 2). Hence, PC1 is used as a reduction of these elements to one single parameter. In contrast Pb contributes about 88% to PC2. PC1 and 2 together account for 63.3% of the variations. The absence of a correlation between Ti as one of the major contributors to PC1 and Pb is not only shown by the PCA itself but also by the correlation coefficient of these two elements (R 2 = 0.01). A low correlation coefficient was also found for Cu and Ti (R 2 = 0.11).

Out of 156 pollen and 48 spore types distinguished, the 35 most significant taxa are shown in a percentage diagram. Also presented are percentages of bryophytes, including Sphagnum and Phaeoceros, and the algae Botryococcus braunii (Fig. 5). Additionally, a summary percentage diagram illustrates 11 different groups of taxa, charcoal data as well as concentrations of pollen and Botryococcus braunii (Fig. 6).
Fig. 5

Pollen percentage diagram of Laguna Campana illustrating the most important and frequent taxa grouped into potential natural vegetation types of páramo, subpáramo, upper mountain rainforest (UMF), lower mountain rainforest (LMF) and semideciduous interandean forest (SDF) together with cultivation and plantation indicators. Taxa with <2% representation are shown by percentage bars with an exaggeration factor of 10×

Fig. 6

Summary pollen diagram showing vegetation groups, concentration data for pollen, charcoal and Botryococcus together with CONISS cluster analysis of the Laguna Campana sediment record

Constrained cluster analysis as well as pollen and XRF data observation resulted in four main zones (LC-I to IV) and one subdivision of the third zone (LC-III a, LC-III b). These zones reflect major environmental changes in the lake and the study area. Displayed pollen taxa with <2% representation are generally not discussed in the text.

Zone LC-I (97–92 cm, 3 pollen samples, base of the record)

Values for PC1 are low in LC-I, being lower only in the most recent sediments of LC-IIIb and LC-IV (Fig. 3). However, there is a distinct rise to the top of this zone peaking at the very bottom of the next zone LC-II. The opposite can be observed for all other parameters: after a clear maximum in LC-I (representing the highest values of the whole record for the inc/coh and Fe/Ti ratios) there is a rapid decline towards LC-II where values bottom out in the lowermost part. In general there is an opposite pattern of PC1 vs. inc/coh which can be observed in the whole record.

The zone LC-I is dominated by very high proportions of páramo taxa decreasing to the top of the zone from 83 to 45%. This is mainly caused by a decrease in Poaceae pollen from 80 to 32%. Cyperaceae pollen contributes to the páramo group with values between 2 and 15%. The low represented subpáramo taxa (7–11%) become more abundant to the top of the zone as shown for instance by pollen of Melastomataceae (0–6%) and Asteraceae subf. Asteroideae (5–9%). UMF taxa first show low pollen percentages of 7% but increase markedly within this zone to 32%. This is mainly due to an initial increase of Alnus pollen from 5 to 24%. Subsequently, Weinmannia pollen appears up to 3%. Pollen of Hedyosmum (1–2%) and Myrica (0–3%) represents other important UMF taxa. LMF taxa show low values (0–3%) mainly of Moraceae/Urticaceae pollen (0–2%). One pollen grain of Zea mays (0.3%) is present in this zone. Pteridophyta spores increase to the top of the zone from 15 to 27%, to which Cyatheaceae and Lycopodiaceae spores contribute up to 2% each. Colonies of the green algae Botryococcus braunii are absent in the bottom sample but increase to the top of the zone up to 3%, reaching a concentration of 8495 colonies cm−3. Charcoal particles (1,290–3,230% relative to the pollen sum) show highest percentages and concentrations (2.3–5.3 million particles cm−3) in this zone. Pollen concentration increases to the top of the zone from 160,000 grains cm−3 to the highest concentration of 326,000 grains cm−3.

Zone LC-II (92–54 cm, 19 pollen samples, base of the record to a.d. 1900)

The highest values for PC1 are followed by a progressive decline towards the top of this zone (Fig. 3). Again, the opposite can be observed for the inc/coh ratio: starting with lowest values of the record it rises continuously. The same applies to Pb and the Pb/Ti ratio respectively. From the bottom of LC-II upwards the Fe/Ti ratio shows only minor variations up to the top of the record. The Cu/Ti ratio presents some kind of cyclical pattern but exhibits no trend (Fig. 3).

Decreased páramo proportions (23–39%) stabilize in this zone, indicated mainly by lower pollen frequencies of Poaceae (19–27%) and Cyperaceae (3–8%). Subpáramo taxa remain stable (4–10%), primarily due to pollen percentages of Melastomataceae (3–9%), Asteraceae subf. Asteroideae (2–10%) and Ericaceae (0–3%). UMF taxa are well represented, but decrease in the upper part of the zone from 46 to 33%. This is mainly caused by a marked increase of Weinmannia pollen from 7 to 29% at the beginning of this zone and a subsequent decrease to 19% in the upper part of the zone. Alnus pollen shows a decreasing trend from 24% to a minimum of 8%. Pollen percentages of Hedyosmum (0–4%), Myrica (1–4%) and Myrsine (1–3%) are stable but lower. LMF taxa are still poorly represented but reach the highest proportion of 13%, mainly through increasing values of Moraceae/Urticaceae pollen from 2 to 7% as well as higher pollen percentages of Alchornea (0–3%) and Acalypha (0–2%). Pteridophyta spores increase slightly to the top of the zone from 15 to 17%, mainly through increasing unknown types (not shown in the diagram). The most frequent known spore types such as Cyatheaceae, Lycopodiaceae and Huperzia (0–2%) remain stable. Sphagnum spores appear and increase to the end of this zone up to 5%. After a distinct increase in the first half of the zone Botryococcus braunii colonies show the highest proportion of 2,452% at a depth of 81 cm and decrease subsequently to 294%. This is mirrored by the concentration data of Botryococcus braunii starting at 20,000 colonies cm−3 at the base of this zone, peaking at 5.5 million colonies cm−3 at 81 cm depth and decreasing subsequently to 400,000 colonies cm−3. Varying charcoal percentages (802–2242%) and concentrations (1.0–4.2 million particles cm−3) show a decreasing trend but the last sample in this zone yields a high value of 2.6 million particles cm−3 which is twice as much as the previous sample. Pollen concentrations decrease slightly to the top of this interval from 283,000 grains cm−3 to 87,000 grains cm−3 parallel to charcoal concentrations. The highest pollen concentration occurs at the same depth as the concentration of Botryococcus braunii colonies peaks.

Zone LC-IIIa (54–34 cm, 10 pollen samples, a.d. 1900–1950)

The trends in element composition described for LC-II continue in LC-IIIa. However, magnitudes are much lower.

Páramo taxa show lower values between 29 and 20% than in zone LC-II, which is primarily due to lower proportions (2–5%) of Cyperaceae pollen. Compared to the top of the previous zone UMF taxa are represented by slightly higher proportions between 38 and 49%, mainly because of higher pollen percentages of Weinmannia (14–26%) and Alnus (10–18%). A first pollen grain of Phaseolus is found in this zone. Sphagnum spores markedly increase to the highest percentage of 14% at the top of the zone, while colonies of Botryococcus braunii continue to decrease markedly reaching very low percentages of 60% and concentrations of 74,000 colonies cm−3. Charcoal particles (783–1,581%) are less frequent than in the previous zone and show stable but low concentrations with a maximum of 1.4 million particles cm−3. The slightly decreasing trend in pollen concentration as observed in the previous zone continues, reaching minimum values of 83,000 grains cm−3.

Zone LC-IIIb (34–26 cm, 4 pollen samples, a.d. 1950–1960)

Apart from those in LC-I, variations in all parameters related to element composition are highest in LC-IIIb. The lowest values in PC1 and Pb are followed by values in the range of the upper part of LC-IIIa. In contrast the highest values of the record in the inc/coh, Pb/Ti and Cu/Ti ratios are followed by much lower values.

In this subzone pollen data are comparable to the previous zone (LC-IIIa). However, UMF taxa decrease from 41 to 36%, most notably due to lower values of Alnus (11–12%) and Myrica (1–4%) pollen. Sphagnum spores show slightly lower values between 7 and 10% than at the top of the previous subzone. Botryococcus braunii colonies show an opposite trend of slightly increasing values to the top of LC-IIIb reaching values of 314% and concentrations of 260,000 colonies cm−3.

Zone LC-IV (26–0 cm, 16 pollen samples, a.d. 1960–present)

LC-IV shows only small variations in PC1 and the inc/coh ratio. Pb, Pb/Ti and Cu/Ti show some changes at high levels.

In this interval greater changes in the pollen composition are observed than in zones LC-IIIa/b. Páramo taxa remain stable between 15 and 27%, but Cyperaceae pollen shows higher proportions (2–7%). Subpáramo taxa increase towards the top reaching highest values of 24%. This is mainly due to higher pollen percentages of Melastomataceae (8–15%) exceeding those of all prior zones. In particular the pollen type of Melastomataceae >25 μm appears for the first time with considerably high percentages and increases markedly to reach a highest proportion of 14% at the top of this zone. A distinct decrease of UMF taxa towards the top from 40 to 28% is primarily due to the marked decline of Weinmannia pollen from 23 to 4%. In contrast Alnus pollen increases slightly from 8% to 18%. LMF taxa (4–11%) and its components such as Moraceae/Urticaceae pollen (3–6%) are stable above zone LC-II. Pinus (0–1%) and Zea mays (0–1%) pollen is more frequent. Pteridophyta spores, mainly unknown types, show higher proportions in the second half of this zone than in all previous zones and reach maximum values of 38%. Spores of Cyatheaceae (0–7%) and Lycopodiaceae (0–3%) do not show notable changes. Sphagnum spores (0–9%) fluctuate inversely to Botryococcus braunii colonies. However, Sphagnum is less important in this zone than in the previous one, while Botryococcus braunii colony percentages increase markedly from 85 to 1,696% to the top. However only slightly higher Botryococcus braunii concentrations of a maximum of 520,000 colonies cm−3 are observed compared to the previous zone. Charcoal particles show high variable percentages (543–1,914%) but concentrations clearly decrease to the top of the zone to the minimum of 108,000 particles cm−3. The same decreasing trend is observed for pollen concentrations reaching their minimum of 13,000 grains cm−3 in the uppermost sample.

Interpretation and discussion

Lake genesis and subsequent vegetation development

Geomorphologic observations suggest that the lake was formed by a shallow landslide forming a dam towards the downhill side of the lake. Due to the high relief energy, with steep slopes resulting in geomorphologic instability, shallow landslides are common in the tropical mountain forest area of the Ecuadorian Andes (Schrumpf et al. 2001; Bussmann et al. 2008; Gradstein et al. 2008). Many gaps without vegetation or with early succession stages of vegetation also indicate erosion and mass movements surrounding the study area (Wilcke et al. 2003).

The fact that it was impossible to penetrate any further into the sediment suggests that the whole sedimentary sequence of Laguna Campana was recovered. A clear separation of a zone of low minerogenic input together with high organics instead of a more mixed signal might indicate that only the uppermost part of the soil horizons were displaced, which become rich in humus towards higher elevations (Gradstein et al. 2008). Removal of the organic layer and the uppermost part of the A-horizons in the head area and redeposition of the material in the foot area is typical of the shallow landslides described in the study area (Bussmann et al. 2008). The highest charcoal percentages and concentrations found in the bottom sample indicate that fires may have played a significant role in soil erosion and furthermore may have triggered the landslide causing lake formation.

Fe/Ti ratios are much lower in the upper part of the record. Therefore, Fe migration within the sediment column appears to be rather unlikely. Hence, we speculate that the iron enrichment in LC-I is a relict of former soil formation processes. Most studies dealing with vertical distribution of metals in soil profiles report a tendency toward concentration in the upper horizons. The surface enrichment of metals in soils may be a result of chemical complexing by organic compounds (Mirsal 2008). Low pH might have caused an upward migration of Fe as acidic and reducing conditions are the most favourable for metal solubilisation (Chuan et al. 1996; Charlatchka and Cambier 2000). Reductive dissolution of clay-sized Fe(III) hydroxides and vertical and lateral leaching of the released Fe was also suggested in an altitudinal transect close to the study area (Wilcke et al. 2008). The same mechanisms might influence Pb/Ti and Cu/Ti ratios. For example for Cu fixation mainly organic substances as well as pedogenic Fe- and Mn-oxides are important, as are pedogenic oxides, notably for Pb enrichment (Hiller and Brümmer 1991; Chuan et al. 1996; Charlatchka and Cambier 2000). As most heavy minerals form complexes with humic acids they are preferentially enriched in the top humus layer or topsoil (Brümmer et al. 1986). Additionally, an enrichment of Pb and Cu in topsoil might be caused by fallout from atmospheric sources before the landslide. Unfortunately, no soil investigations have been carried out in our study to verify this hypothesis of Fe, Pb and Cu enrichment in topsoil. Although soil development might vary considerably between the warm and humid eastern side of the Cordillera Real (Beck et al. 2008b), investigations on the western part showed reddish subsurface horizons indicating redoximorphic processes (Beck et al. 2008b) or an enrichment of Fe at least in the A-horizon (Schrumpf et al. 2001). Therefore, if this scenario is valid for the study site it provides a hint that the bottom of the record is formed by the upper part of a displaced soil and that the whole sediment sequence was recovered. If there had been a number of slumps rather than just one, the data suggests that at least the last event was recovered completely.

According to the two lowermost radiocarbon dates which probably represent the formation of Laguna Campana the respective landslide has a terminus post quem of ~a.d. 1470. This indicates that landslides already occurred during this time. As the landslide removed the vegetation cover from a large part of the catchment of Laguna Campana, this probably led to further erosion which is mirrored by minerogenic input. Increased post-landslide erosion on sparsely vegetated landslide areas was also previously observed by Bussmann et al. (2008). After vegetation recovery erosion and hence minerogenic input decreases in LC-II (Fig. 3).

Further evidence for a complete recovery of the sediment sequence deposited in Laguna Campana comes from pollen analysis representing mainly local vegetation changes. The bottom sample showed very high percentages (up to 80%) of Poaceae, indicating that the vegetation at the disturbed area most likely consisted of high Poaceae proportions before the landslide occurred. As the surroundings after the landslide probably still held vegetation rich in grasses, these could quickly become established in the area. It seems that during this first successional stage other vegetation components were initially suppressed by the dense grass layer. This is supported by studies of Bussmann et al. (2008), showing that on landslides grasses build a dense layer and limit the establishment of bush species. The high Poaceae presence of ~20% persisting after the initial peak represents a remaining above-average grass proportion in the study area, as such high grass abundances normally occur in much higher elevations where páramo is found (Weng et al. 2004a).

After this first establishment of grasses, vegetation succession began, even though a high proportion of grass remained. Cyperaceae grew up in wet locations such as small ground depressions and watersides. At the same time pioneer trees of Alnus, here Alnus acuminata, expanded on moist and probably disturbed sites (Weng et al. 2004b) and their pollen reached its highest proportion of 24% in an early successional stage. Some Alnus pollen could have originated at lower elevations and might have been dispersed to higher altitudes, but as pollen proportions never fell below 5% it probably reflects local occurrence (Weng et al. 2004a). Ongoing vegetation regeneration led to an expansion of Weinmannia up to ~30% in the beginning of zone LC-II, while Alnus declined over the same interval. As different species of Weinmannia have a large altitudinal range in the study region of the Podocarpus National Park (Lozano et al. 2003; Homeier and Werner 2008), Weinmannia pollen could have been transported by wind. However, most species occur in the UMF and subpáramo zone (Niemann et al. 2009) and studies carried out in New Zealand (Moar 1970) revealed that high pollen frequencies of Weinmannia certainly imply local dominance. Based on that, the high pollen presentation of Weinmannia probably indicates that this genus contributing to the upper mountain rainforest recovered in the area to a certain extent, possibly due to decreasing human disturbances. Mainly Hedyosmum, Myrica and Myrsine were associated with dominating trees of Weinmannia. Together with Melastomataceae and Asteraceae this vegetation composition constituted a considerable part of the local vegetation. Woody plants probably represented small trees and shrubs in the understory. Myrica and Myrsine also are pioneer species, indicative of disturbance.

A high occurrence of pteridophyta was established rapidly during the successional stages of Alnus and Weinmannia and increased throughout the whole record from 6 up to 38%. This gives an indication of vegetation structure, as ferns may be characteristic of a wet understory but also show high occurrences on open soils after disturbance (Bussmann et al. 2008). Hence, pteridophyta at Laguna Campana indicate most likely sparse vegetation on open soils or subsequently open secondary forests stands. This converted vegetation composition probably harbors much less biodiversity than undisturbed natural UMF occurring elsewhere.

Anthropogenic impact and further vegetation changes

A crucial factor for the vegetation development at Laguna Campana is human influence. Already the bottom sample showed the highest charcoal percentage of 3,230% relative to the pollen sum and the highest charcoal concentration of 5.3 million particles cm−3, indicating high fire frequency. Former studies in the Podocarpus National Park region concluded that increasing fire frequencies during Holocene times were most likely of anthropogenic origin. Common fires during late Holocene times concurrent with high grass pollen occurrence have been previously interpreted as indication of early human activities (Niemann and Behling 2008a; Niemann et al. 2009).

Given the fact that fires were used for slash and burn purposes (Niemann and Behling 2008a) a natural cause for fire is probably negligible. During the whole duration of the record fires occurred and affected the vegetation. These might have been more intense in this area, compared to more easterly located sites in the PNP, due to drier climatic conditions. The lower charcoal concentration in the uppermost zone (LC-IV) probably does not reflect decreasing fire frequency. Charcoal percentages similar to those in previous zones suggest rather constant fire occurrences. The high water content and lower sediment compaction in the top samples may be responsible for the lower concentration data calculated per sampled volume. This applies to charcoal as well as pollen concentrations. The initial high proportions of Poaceae after the landslide may also indicate human impact. As Bussmann et al. (2008) described, a first succession of a dense grass layer occurs particularly on anthropogenically caused landslides and differs from that on natural ones. Human land use had already opened up the vegetation cover before the landslide event and probably reduced the local biodiversity. This could have favored Poaceae distribution at elevations up to 2,500 m a.s.l., where naturally UMF dominates.

A marked decrease of Weinmannia during very recent times also indicates human activities. High fire frequencies strongly reduce the occurrence of Weinmannia (Niemann and Behling 2009). As burning for forest clearance or new farming areas is still a common method used by settlers and has been so for centuries (Beck et al. 2008c), Weinmannia may have been seriously affected by these fires during the last decades. This supports the assumption that fires remained frequent in the zone LC-IV. Additionally, Weinmannia might have been the target of timber extraction. Concurrently with the decline in Weinmannia during most recent times, Melastomataceae has increased markedly. While the pollen type including all Melastomataceae <25 μm only expanded slightly (8-15%) in the uppermost zone, the pollen type >25 μm occurred for the first time in high abundances. The high pollen input from Melastomataceae >25 μm probably originated from a local stand of Melastomataceae at the shore of Laguna Campana observed during field work.

Furthermore, the crop plant Zea mays and the domesticated wild bean Phaseolus, already present in zone LC-I, evidence permanent land use in the area. Ancient human settlements have taken place in the area since ~4000 years cal b.p. (Guffroy 2004). The Inca occupied the area of Loja and Zamora in the middle of the fifteenth century. During their 70-year rule in southern Ecuador (a.d. 1463–1531) the indigenous group of the Saraguros was brought to the Ecuadorian highlands. Their traditional mixed cultivation system featured maize, beans, potatoes and other tubers. As early as the nineteenth century cattle breeding supplemented their livelihood (Pohle 2008).

However, lower abundances of cultivation indicators found throughout the zones LC-I to LC-III suggest a phase of less human activity compared with that in most recent times. This is supported by another nearby palynological study, in which the time period between the seventeenth and twentieth centuries was identified as a phase of lower human activity (Niemann and Behling 2008a). Thus in particular, the more frequent Zea mays pollen found in zone LC-IV suggests expanded cultivation during the last decades. This may be related to mestizo settlements in the study area founded during the acceleration of the Latin American Industrialization in the mid twentieth century (Niemann and Behling 2008a; Pohle 2008). Nowadays agriculture is still the most important economic activity in southern Ecuador. In the Loja province 44% of the economically active population works in agriculture (INEC 2001). Population pressure and improved infrastructure have opened even ecologically unsuitable areas to agricultural colonization during the past 50 years (Pohle 2008). The low amount of canopy trees like Clethra and Podocarpus found in the pollen diagram probably results from the fact that they were already objectives for wood extraction in the mid sixteenth century after the Spanish conquest (Guffroy 2004), mainly for the construction of the city of Loja.

Pinus pollen found in the record gives evidence of European influence in the study area. Pines were introduced only after colonization of the southern hemisphere by Europeans (Richardson 2000) at the beginning of the 20th century. Today large stands of introduced Pinus can be found in some areas of the Inter-Andean valleys (Neill 1999). Pinus pollen found more frequently in the uppermost zone LC-IV confirms the expansion of plantations during the last decades.

Although the present vegetation near Laguna Campana is composed of a considerable proportion of Puya, pollen of Puya is poorly represented in the pollen diagram because of its rare flowering. However, Puya pollen was found in samples from the lower zones as well as in the most recent samples. Apparently, Puya was already part of the vegetation around Laguna Campana in former times and persisted till today. Puya observed in the field seems to be fire resistant, which probably favored long term existence in this area.

A different kind of human impact seems to be reflected by heavy metals. The increase in Pb/Ti ratio from the bottom to the top of the record indicates enrichment in Pb relative to Ti. As Ti, which is represented by PC1 in Fig. 3 decreases continuously, the increase in the ratio might also be caused by a constant supply of Pb which is independent of the supply of lithogenic input. However, absolute counts for Pb also show an increasing trend over the record. Chemical diagenesis seems to be of minor importance as above the peak in LC-I the Fe/Ti ratio varies only little. If Pb had migrated upwards in the profile, variations would have been observed in the Fe/Ti ratio as Pb is less mobile than Fe (Charlatchka and Cambier 2000; Dorronsoro et al. 2002). There is also a growing body of information for ombotrophic peat bogs suggesting that Pb is immobile in this environment (Shotyk et al. 2005). The continuous rising trend of Pb from the bottom to the top of the record impedes the calculation of an enrichment factor because no natural background deposition of Pb was recovered in the record. As the XRF Scanner provides only semi-quantitative data, it is neither possible to obtain absolute inputs nor distinguish between lithogenic and anthropogenic components in the same way as has been done in previous work (Shotyk et al. 2001, 2005; Koinig et al. 2003). Nevertheless, the rise in Pb and Pb/Ti respectively suggests an enrichment of Pb independent of lithogenic supply from the beginning of the record. Since chemical diagenesis does not seem to have been the driver we suggest an increased atmospheric supply in this case as the atmospheric loading is especially important for lead. It is estimated that over 95% of the lead is of anthropogenic origin (Salomons and Förstner 1984). Similar observations have been made in lakes and peat profiles in Europe (e.g. Hettwer et al. 2003; Koinig et al. 2003; Shotyk et al. 2005; Guyard et al. 2007) and other South American countries like Peru or Bolivia (Abbott and Wolfe 2003; Cooke et al. 2007, 2008).

Distinct Pb anomalies were attributed to long range transport of atmospheric Pb contamination from Pb mining and smelting during Roman times in Europe (Hettwer et al. 2003; Shotyk et al. 2005; Guyard et al. 2007). The same studies show an even more distinct Pb peak related to the introduction of aerosols from leaded gasoline combustion or coal burning (Koinig et al. 2003; Shotyk et al. 2005). In Bolivia and Peru atmospherically derived input is also associated with smelting processes. Following the Inca conquest of the Andes ~a.d. 1450, marked increases in Pb are noted at all study sites and after the Hispanic conquest, large increases in Pb pollution are noted, only to be superseded by industrial development (Cooke et al. 2007, 2008). The source of the lead in the study area remains to be identified, but combustion can be assumed at least during subrecent times. Surprisingly, there is no contemporaneous rise in Cu from LC-I to LC-IIIa. Although there are variations, it remains in the same range. Only in LC-IIIb (~a.d. 1950) is there a distinct rise in Cu/Ti which is contemporaneous with the highest values in Pb/Ti but also the lowest values in PC1 and Pb. This either indicates a further increase in the atmospheric supply of heavy metals or a greater dependence of the ratio signal on lithogenic input. Elevated Cu and Pb contamination was found close to small scale gold mining areas in southern Ecuador, such as in the Nambija region approximately 20 km east of the study site. The main gold rush started there during the 1980s but due to different extraction methods primarily waterways have been affected by the main contaminants which consist of Cu, Pb and Cd (Swedish Environmental Systems 1999; Tarras-Wahlberg et al. 2000).

Hydrological variations

Minerogenic input (PC1) is probably related to lake level variations as higher precipitation causing higher lake levels will also cause an increase in erosion (Haberzettl et al. 2007). The green algae Botryococcus braunii is known to thrive in freshwater bogs, temporary pools, ponds and lakes (Batten and Grenfell 1996). In other studies Botryococcus has already been used as indicator of open water conjoined with other indications (Davis 1999; Niemann and Behling 2009). Higher Botryococcus presence is mostly coupled with increases in PC1 values in the record (Fig. 7). Accordingly, both are interpreted as occurring concurrently with increased moisture availability. In some cases increased PC1 values are observed without an increase in Botryococcus. This is probably caused by single erosion events which did not have a longer lasting impact on the lake level. Interpretation is implemented by the occurrences of Sphagnum as an additional indicator, meaning a higher presence of Sphagnum for periods with lower water level and hence variations in precipitation.
Fig. 7

Comparison of Principle Component 1 (-PC1, 3-point moving average) representing minerogenic input and Botryococcus colonies related to the total pollen sum

Botryococcus was absent in the bottom sample and started to increase markedly to its highest percentages and concentrations in the lower part of zone LC-II, indicating that the Laguna Campana water level rose quickly after the landslide event. Despite an increasing input of organic material Sphagnum was virtually absent in this period. Therefore the water level must have been high.

The landslide also was probably triggered by very moist conditions, which indicates that the lower part of the record is the wettest. Unfortunately, during the highest occurrence of Botryococcus in LC-II the PC1 signal is overprinted by the vegetation development in the catchment area. Hence, the high but decreasing PC1 values in this depth are probably a response to the developing vegetation cover and only marginally caused by hydrological variations.

After a steep decrease Botryococcus stabilizes. Together with the first re-increase in PC1, this points to still wet conditions. However, with the beginning of Sphagnum development a change to somewhat drier conditions is suggested. The trend of drier conditions continued over the zones LC-IIIa/b, related to the time period of ~a.d. 1900–1960. The driest conditions then occurred during the transition between zone LC-IIIa and b around a.d. 1950, when Botryococcus showed its sparsest presence, Sphagnum reached its highest proportions and PC1 yielded its lowest values. At this time the peat moss Sphagnum started to expand and peat bogs arose in the littoral areas.

A marked increase in PC1 values from zone LC- IIIb (~a.d. 1960) onwards reflects a return to more humid conditions probably because of higher precipitation during the last ~50 years. During the most recent period Botryococcus expanded and Sphagnum was suppressed because of a lake level rise. Although the Botryococcus concentration did not increase markedly in LC-IV, which is probably related to the low sediment compaction, the Botryococcus to pollen ratio gives information about a relative but distinct rise. Additionally, the highest proportions of pteridophyta during this time, including a considerable presence of tree ferns of the genus Cyatheaceae (0–7%), support wetter climates.

Conclusions

The multi-proxy approach provided an ample environmental reconstruction combining multiple indicators of human impact and past processes inducing lake genesis and vegetation development. Laguna Campana originated from a shallow landslide which displaced only the uppermost soil horizons. The terminus post quem for the occurrence of the landslide which might have been promoted by anthropogenic impact is a.d. 1470. Humans influenced the study area and its vegetation continuously by slash and burn practices, pastures and deforestation at least for the recorded time period and especially during most recent times. Therefore, a dense mountain rainforest could not recuperate in the area. This means that a vegetation structure with diminished biodiversity compared to natural conditions might be similar to the present appearance since the formation of Laguna Campana. An anthropogenic impact can also be concluded from the continuous rise of lead, which can hardly be explained by natural input.

Reconstructed hydrological variations probably caused by variations in precipitation affected riparian vegetation but had no major influence on the vegetation at a greater distance from the lake. However, the wettest conditions probably triggered the landslide and the driest conditions during a.d. 1900-1960 induced local peat bog development in the littoral.

Notes

Acknowledgements

We wish to sincerely thank Antoine Cleef, Urs Neumeier, Hans Ruppert and Guillaume St-Onge for fruitful discussions. We also acknowledge Fernando Rodriguez and Isabelle Matthias for support during field work. We would like to thank the associate editor Eric C. Grimm and two anonymous reviewers for their comments which improved an earlier version of the manuscript. Torsten Haberzettl was supported by a postdoctoral fellowship scholarship provided by Le Fonds Québécois de la Recherche sur la Nature et les Technologies (FQRNT). The Deutsche Forschungsgemeinschaft (DFG) is thanked for financial support within the research group FOR 816 (Be 2116/8-1). Logistic support was kindly provided by the staff of FOR 816.

Open Access

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Copyright information

© The Author(s) 2010

Authors and Affiliations

  • Corinna Brunschön
    • 1
    Email author
  • Torsten Haberzettl
    • 2
  • Hermann Behling
    • 1
  1. 1.Department of Palynology and Climate Dynamics, Albrecht-von-Haller Institute for Plant SciencesUniversity of GöttingenGöttingenGermany
  2. 2.Department of Physical Geography, Institute of GeographyFriedrich-Schiller-University JenaJenaGermany

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