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Revista chilena de historia natural

versión impresa ISSN 0716-078X

Rev. chil. hist. nat. v.80 n.2 Santiago jun. 2007

http://dx.doi.org/10.4067/S0716-078X2007000200002 

 

Revista Chilena de Historia Natural 80: 141-156,2007

ARTÍCULOS/ARTICLES

 

Changes of sub-fossil chironomid assemblages associated with volcanic sediment deposition in an Andean lake (38°S), Chile

Cambios en las asociaciones sub-fósiles de quironómidos, producto de la depositación de sedimentos volcánicos en un lago andino (38°S), Chile

 

ALBERTO ARANEDA1-2*, FABIOLA CRUCES3-1, LAURA TORRES3-1, SEBASTIEN BERTRAND4, NATHALIE FAGEL4, HANS C. TREUTLER5, LUIS CHIRINOS1-6, RICARDO BARRA2 & ROBERTO URRUTIA1-2

1 GEP (Grupo de Estudios Paleolimnológicos), Unidad de Sistemas Acuáticos, Centro EULA Universidad de Concepción, Casilla 160-C, Concepción, Chile
2 Unidad de Sistemas Acuáticos, Centro EULA Universidad de Concepción, Chile
3 Departamento de Botánica, Universidad de Concepción
4 Clays and Paleoclimate Research Unit, Department of Geology, University of Liege, Belgium
5 UFZ-Centrum, Leipzig, Germany
6 Departamento de Ingeniería, Pontificia Universidad Católica del Perú, Perú


ABSTRACT

Chironomid assemblages and sedimentological parameters (grain size, organic content, mineralogy) of a short sediment core from Lake Galletué (38°41' S, 71°17' W) were analysed. The sedimentary record includes one volcanic ash (tephra) layer, which has a completely different composition than the host sediment in terms of organic content, grain size, and mineralogy. According to the geochronology (210Pb and 137Cs), this ash layer corresponds to the eruption of Llaima Volcano in 1956-1957. The tephra deposition had an impact on chironomid assemblages producing, among other changes, an increase in Parakiefferiella and a decrease in Ablabesmyia, although no noticeable change was detected in the diversity index. When compared with other studies, our results also show an impact in terms of the presence of chironomid head capsules within the tephra. The presence of these head capsules could result from the effects of percolation, since the coarse grain size of the tephra particles provides large interstitial spaces. The recovery in the abundances of some taxa after the tephra input, suggests the lake is probably restoring the conditions prevailing before the tephra fall.

Key words: chironomids, lake sediments, tephra layer, southern Chile.

RESUMEN

Se analizan las asociaciones de restos sub-fósiles de quironómidos y los parámetros sedimentológicos de un núcleo sedimentario del lago Galletué (38°41' S, 71°17' O). Es evidente en este núcleo la presencia de un estrato de sedimentos volcánicos (tefra) de una composición distinta en el contenido deµmateria orgánica, en el tamaño de partícula y en la mineralogía, respecto de los sedimentos del lago. De acuerdo a la geocronología isotópica (210Pb y 137Cs), los sedimentos de esta tefra podrían corresponder a la erupción del volcán Llaima de 1956-1957. Por otra parte la depositación de esta tefra también provocó un cambio en las asociaciones de quironómidos, siendo evidente el aumento de Parakiefferiella y la disminución de Ablabesmyia dentro del estrato de tefra. Si bien nuestros resultados, al igual que estudios previos, registran un cambio en las asociaciones de quironómidos debido a la entrada de sedimentos volcánicos, un aspecto diferente es la presencia de cápsulas cefálicas dentro de la tefra. Una posible explicación a tal diferencia podría ser la percolación de los restos de quironómidos por los espacios intersticiales de la tefra. La recuperación en la abundancia de algunos taxa luego de la depositación de la tefra, sugiere que el lago restablecería las condiciones existentes previo a la caída de la tefra.

Palabras clave: quironómidos, sedimento lacustre, estrato de tefra, Chile.


INTRODUCTION

Chironomids (Insecta: Diptera) have been used extensively,µmainly in the northern hemisphere, to study the past climate, trophic status of lakes, oxygenation levels, and water quality, among others (Walker 1987, Walker et al. 1991, Walker et al. 1995, Heinrichs et al. 1997, Olander et al. 1997, Brooks & Birks 2000, 2004, Brooks et al. 2001, Larocque et al. 2001, Little & Smol 2001, Quinlan & Smol 2001, Adriaenssens et al. 2004). These insects make good paleolimnological indicators because they are abundant inµmany water bodies, the larval head capsules preserve well in sediments, and the winged adult stages are highly mobile, enabling them to disperse over wide areas (Brooks 2000, massaferro & Brooks 2002). Despite their usefulness as environmental indicators, chironomids are rarely used as such outside of the Northern Hemisphere, especially not in southern South America, where only a few studies focus on this insect group.

Specifically in Chile, little is known about the taxonomy and paleo applications of chironomids. Brundin (1983) identified a new sub-family for Chile, Chilenomyiinae, comprising only one species: Chilenomya paradoxica. Later, Arenas (1995) studied the composition and distribution patterns of zoobenthos in the Biobio River, identifying 25 chironomid taxa; the genus Cricotopus occurred throughout the river. Andersen (1996) described a new chironomid species, Monodiamesa mariae, from southern Chile (Los Palos River; 45°23' S, 72°41' W).

Recently, massaferro et al. (2002) found 49 chironomid taxa at Laguna San Rafael National Park (46° S). The subfamily Orthocladiinae was clearly predominant, followed by Tanypodinae, Podonominae, and Chironominae. In another work, massaferro & Brooks (2002) carried out the first study of sub-fossil chironomid assemblages in Chile at Laguna Stibnite (46°25' S, 74°24' W), relating chironomid assemblages to environmental changes developed during the Late Quaternary. The authors found 34 chironomid taxa that reflected environmental changes throughout the Late-glacial and the Holocene.

Only a few references address the impact of volcanic eruptions on chironomid assemblages and other aquatic biota in South America (Massaferro & Corley 1998, massaferro et al. 2005), although Eastwood et al. (2002) found that volcanic eruptions can have substantial impacts on natural ecosystems and that volcanic depositions provide an opportunity to evaluate species interactions and ecosystem resilience (Lotter & Birks 1993, Barker et al. 2000).

Some studies, mainly in the Northern Hemisphere, have focused on evaluating ecosystem responses to volcanic impacts. Birks & Lotter (1994) described the changes in diatom assemblages after a tephra deposition near Laacher See volcano, Germany. Changes in diatom production were found in British Columbia as an effect of tephra deposition (Hickman and Reasoner 1994). Heinrichs et al. (1999) reported changes in chironomid assemblages at Kilpoola Lake (British Columbia) after the deposition of an ash layer, and Tsukada (1967) found decreased abundance of Tanytarsus genuinus after two events of volcanic sediment deposition in Lake Nojiri, Japan. Recently, massaferro et al. (2005) used chironomid assemblages to reveal short term environmental changes in Lakeµmorenito of the Argentinean Patagonia (41° S, 71° W), with volcanism being the most important factor affecting the chironomids.

The principal aim of this study was to record the changes in chironomid assemblages after a volcanic event (tephra layer) using a short sediment core from Lake Galletué (Region IX); this is the first study of sub-fossil chironomid assemblages from an Andean lake in Chile. The study of how a volcanic event could affect chironomid assemblages is important as it allows us to disentangle this response from other environmental impacts.

MATERIAL AND METHODS

Study site

Lake Galletué (Fig. 1) is located at 38°41' S, 7Io 17' W in central Chile at an altitude of 1,150 µm. It is approximately 26 km from the nearest city, Lonquimay. The lake has a surface of 12.5 km2 and the maximum depth is 45 m. It is an oligotrophic, monomictic temperate lake with summer stratification (Parra et al. 1993). The lake experiences a steep seasonal gradient in air temperature with extremes of -6.0 °C in winter and 28.9 °C in summer. Annual average precipitation is 1,900 mm with a maximum of 3,018 mm and a minimum of 1,180 mm (Parra et al. 1993).


Fig. 1: Study site indicating the location of Lake Galletué.

Área de estudio indicando la localization del lago Galletué.

According toµmardones et al. (1993), different vegetational associations are found in the Lake Galletué watershed. A typical temperate rainforest composed mostly of Nothofagus pumilio (Poepp. & Endl.), Nothofagus dombeyi ((Mirb.) Oerst.), and Araucaria araucana ((Mol.) K Koch) covers the north-north eastern portion of the watershed, with upper levels of this forest reaching 35 to 50µm high. The mid-levels are composed mainly of young individuals of the same species, whereas the understorey is dominated by Berberís spp. (michay), Drimys winteri var. andina, and the Chilean bamboo Chusquea sp. (quila). The east-south eastern section of the watershed is covered with a high prairie grassland, called "coironal" that covers important areas of the prairie next to the lake and grows in a cushion form called "champas".

The typical composition of this association isµmarked by the predominance of Festuca scabriuscula (Phil.), Acaena sericea (Jacq.fil.), Baccharisµmagellanica (Radin), and Rumex acetosella (Linnaeus). This community of low vegetation can be also mixed with Nothofagus antárctica (G. Forster, Oerst.) and A. araucana forests. In the wetland zones near the lake, Juncaceae and Ciperaceae species occur together with the herbaceous genera Trifolium,µmelilothus, and Caltha (Mardones op. cit.). These communities indicate the lake has relatively pristine vegetation in its surrounding areas.

Sampling and physical analysis

A Lowrance X-16 echo sound profiler was used to locate the maximum depth of the lake and a 17-cm sediment core was retrieved using an Uwitec gravity corer with a plexiglass tube (6 cm diameter). Later, the core was sliced at 1 cm intervals.

In order to assess the lithology, the core was x-rayed (at 50 kV and 26-30 mA s-1) following the method outlined by Axelsson (1983). The x-ray inspection clearly identified a high reflectance sediment layer, which was separated for mineralogical analysis. The chemical composition (major elements) of this sediment layer was determined using an electron microprobe (Cameca SX50) at the Centre d'Analyse par microsonde pour les Sciences de la Terre, Louvain-la-Neuve University (CAMST). The accelerating voltage was 15 kV and the beam current was 20 nA. Counting times were 20 sec for all elements.

For grain size analysis, samples were sieved at 4.0 and 1.0 phi units in order to separate the sample into fine (mud) and coarse (sand) fractions. Grain size was analyzed using an Elzone 282 PC Coulter Counter particle analyzer. The organic content in each layer was estimated by loss on ignition (LOI) following theµmethod described by Boyle (2002).

Geochronology

The age of the core was determined through the activity of 210Pb. The gammaspectrometricalµmeasurements were done using an HPGe detector with a 0.5µmm beryllium window and an energy resolution of 570 eV at the level of 122 eV. The detector and theµmeasuring geometry were calibrated with certified referenceµmaterial (RGU-1, RGth-1, RGK-1) from the International Atomic Energy Agency (IAEA). Once the activity of each sample was obtained, the age models CIC and CRS (Appleby & Oldfield 1978) were evaluated in terms of age-depth profile and coherency with the peak in 137Cs activity. The CIC was theµmost adequateµmodel. The estimated age was validated with the peak in 137Cs activity, which was observed around 1963, when large quantities of this isotope were released into the atmosphere from nuclear weapons tests (Longmore et al. 1983).

Chironomids

For the chironomid analysis, 4 ml of wet sediment were deflocculated in 10 % KOH for 15 minutes at 70° C and passed through a 90 \im sieve. Later, the remains were transferred to a Bogorov counting tray and head capsules were picked out with entomological forceps. Each head capsule was dehydrated in 80 and 100 % ethanol and then mounted, ventral side up, in euparal. The insects were identified using a Zeiss microscope (25, 40, or 100 x) and the keys of Hofmann (1971), Wiederholm (1983), Epler (2001), Paggi (2001), and Rieradevall & Brooks (2001).

The relative abundance of each taxon was presented as a percentage of the total abundance in each centimetre using the programs TILIA and TILIA GRAPH. To distinguish different associations along the profile, a stratigraphically constrained sum-of-squares cluster analysis (CONISS) was applied. Zonation was applied when examining major differences in CONISS groupings; their significance levels were evaluated with a one-way analysis of similarities (ANOSIM), with zones as factors using the program Primer E.v. 6.12 (Clarke & Gorley 2005). This analysis tests for differences among factors using permutation and randomizationµmethods based on the similarity matrix Bray-Curtis (Clarke et al. 2005). At the same time to determine which taxa were theµmost important in to contribute to the differences among the groups, we used the similarity percentage procedure (SIMPER; Primer v.5, Clarke & Gorley 2001) on transformed variables. In order to relate chironomid assemblages to environmental variables, ordination analyses were performed using the programs CANOCO and CANODRAW. Chironomid diversity and equitability were estimated through the Shannon index, using the program BioDiversity v2.

RESULTS

Physical parameters

The radiograph of the Lake Galletué sediment column is depicted in Fig. 2A. A clear high reflectance sediment layer (white area) present between 7 and 12 cm indicates higher density than in the rest of the core. A first visual inspection revealed coarse, dark, irregular, and very sharp particles, probably belonging to a tephra layer. According to the microprobe analysis, the chemical composition of this tephra corresponds to basaltic andesite with 54.29 % Si02 and 4.32 % Na20 + K20.

The organic content (LOI) follows a trend related to the tephra layer (Fig. 2B), with a noticeable decrease in the section of core where the tephra layer is evident (7-12 cm). The highest organic content (17.2 %) was found at 6 cm, and the lowest (2.3 %) at 10 cm (within the volcanic layer). The lower organic content in the volcanic layer is due to its inorganic nature.


Fig. 2: Physical parameters of Lake Galletué sediment core. (A) X-rays, (B) organic matter, (C) grain size, (D) 210Pb activity, (E) 137Cs activity, and (F) age versus depth profile.

Parámetros físicos del núcleo sedimentario del lago Galletué. (A) rayos-x, (B) materia orgánica, (C) tamaño medio, (D) actividad de 210Pb, (E) actividad de 137Cs y (F) perfil edad versus profundidad.

Grain size analysis (Fig. 2C) shows an increase in particle size in the tephra layer, passing texturally from silt to sand (mean size 6.83 phi = 8.8 µm to 2.16 phi = 223 µm). a more detailed description of the grain size of this tephra is presented in Fig. 3, where two populations of particle sizes are evident. The coarser population corresponds to the tephra layer, with a mean size around 600-900 µm, and the finer population belongs to the host sediment with a diameter below 63 µm. Also, the circular diagrams indicate that the lower sample (11-12 cm) has the highest proportion of mud. Below the tephra layer, the sediment is composed mainly of silt (Fig. 2C).


Fig. 3: Grain-size distribution of the five centimetres where the tephra layer is evident; pie diagrams indicate sand-mud proportion. The lower sample (11 cm) has the highest proportion of mud, reflecting the initial mixing of tephra particles (coarse) with the host sediment (fine).

Distribución del tamaño medio de los sedimentos en los cinco centímetros donde es evidente la tefra. Los diagramas circulares indican la proporción arena/fango. El centímetro inferior (11 cm) tiene la proporciónµmás alta de fango, reflejando la mezcla inicial de las partículas de tefra (gruesas) con el sedimento lacustre (fino).

The activity of 210Pb and 137Cs are presented in Fig. 2D and 2E, respectively. The activity of 210Pb shows a general decreasing trend toward the deepest part of the core. However, some reversal of the 210Pb activity can be seen in centimetres 2, 3, and 4 with respect to the first and fifth centimetres. 210Pb activity is highest (375 Bq kg1) in the first cm and lowest at 16 cm (8.0 Bq kg-1). The total 210Pb inventory in the core reached 2,351 Bq kg-1, indicating that the total flux of 210Pb to the sediments is 73.2 Bq m -2 yr-1. The 210Pb profile reveals an evident relationship with the stratigraphy, as 210Pb activity decreased after the tephra deposition. This drop could be explained by a dilution of 210Pb due to an abrupt input of volcanic sediments into the lake. The uniform mineralogical composition of the tephra layer implies that this input had the same origin and was generated in a relatively short period of time (Fig. 2F).

The 137Cs activity (Fig. 2E) is detectable as of 4 cm (19.0 Bq kg1) and peaks at 7 cm (35.0 Bq kg1). From 10 to 17 cm, the activity is not detectable. According to Longmore et al. (1983), the peak in 137Cs activity probably represents the year 1963, when this radioisotope was released in large quantities during nuclear weapons tests. There is good agreement between the 137Cs and 210Pb profiles.

Chironomid assemblages

A total of 23 chironomid taxa (sub-families Chironominae, Tanypodinae, Orthocladiinae, Podonominae) were identified in the sediment column of Lake Galletué. Theµmost important sub-family in terms of abundance was Chironominae, composed of the tribes Tanytarsini (25.7 %) and Chironomini (11.4 %), and reaching 37.1 % of the total. The second sub-family in importance was Tanypodinae (29.1 %), followed by Orthocladiinae (27.1 %). The sub-family Podonominae had a very low abundance (0.3 %). Unidentified remains represented 6.3 % of the total. Two different groups of Tanytarsini (types A and B) were distinguished based on differencesµmainly in the shape of antennal pedestal. Type A is characterized by an antennal pedestal with a low and rounded spur, whereas Type B has an antennal pedestal with a longer rounded spur at an obtuse angle to the pedestal.

The chironomid assemblages in the Lake Galletué sediments are presented in Fig. 4. Using CONISS analysis, three zones were distinguished in the chironomid assemblages. Zone I (17-12 cm) before the impact of the tephra layer, Zone II (12-6 cm) during the impact, and Zone III (6-1 cm) after the impact. The one way ANOSIM analysis, indicated significant differences among the taxa abundances of the zones identified by CONISS (ANOSIM, RGlobal = 0.36, P = 0.001) and in the paired comparisons (RZonesiiMi= 0.41, P = 0.002, Rzonesµm-i = 0-44, P = 0.002). The SIMPER analysis showed that theµmost important taxa in to determinate differences among zones were Parakiefferiella, Ablabesmyia, Tanytarsini types A and B, Cricotopus/Orthocladius and Macropelopia (Table 1).


Fig. 4: Chironomid percentage diagram, showing the assemblage structure of Lake Galletué sediments. The stratigraphical division was made following CONISS analysis.

Abundancia porcentual de quironomidos en el registro sedimentario del lago Galletué. Las divisiones estratigráficas se realizaron en base al análisis CONISS.


Zone I (17-12 cm) pre-impact

Ablabesmyia (Johannsen 1905) is relatively abundant in this zone, decreasing at 16 cm and 13 cm. Macropelopia (Thienemann 1916) is at its highest abundance (11 %). Other taxa with high abundance in this zone are Parakiefferiella (~20 %) (Thienemann 1936), Tanytarsini type A (35 %), and unidentified remains of Orthocladiinae (12 %). Pseudochironomus (Malloch 1915) only occurs in this zone but with very low abundances (7 %). The number of head capsules found in this zone is relatively high compared to the other zones, reaching ca. 15 heads per ml of wet sediment in some levels.

Zone II (12-6 cm) during the impact

In this zone, the Ablabesmyia abundance decreases, reaching its lowest value at 8 cm (6.8 %). Above 7 cm, it starts to increase gradually. Macropelopia is at its lowest abundance in this zone (3.0 % average). Tanytarsini Type A decreases at the beginning of the zone, showing a transitory increase at 8 cm (17 %). Tanytarsini Type B is absent in the first part of this zone, appearing at 11 cm, and increasing at the end of the zone (14.6 %). Another taxon that decreases gradually in abundance in this period is Cricotopus/Orthocladius (Wulp 1874). However, the greatest change in this zone is the increase of Parakiefferiella starting at 11 cm, reaching abundances considerably higher than those found in the pre-impact zone (25 %). The highest abundances of head capsules were found before the tephra deposition; a noticeable drop is evident immediately after the event (13-10 cm), followed by an increase and subsequent decrease at 8 and 6 cm, respectively.

Zone III (6-1 cm) post-impact

After the tephra deposition, some taxa start to increase rapidly. Ablabesmyia rises after 5 cm, reaching its maximum at 3 cm (36.8 %). Following the impact, both Macropelopia and Parachironomus (Lenz 1921), as well as other unidentified Tanytarsini and Tanypodinae also increase (11.1 and 26 %). However, one of theµmost noticeable changes after the volcanic event is the decrease of Parakiefferiella, which had its highest abundance within the tephra layer. The total number of head capsules shows an increase at 4-5 cm and a decrease towards the uppermost surface sediments.

On the other hand, the diversity estimated by the Shannon index just shows slight changes along the profile. Theµmain drops in chironomid diversity are in the centimetres 15, 12, 6, and 3, with the decrease at 12 cm corresponding to the deposition of the volcanic sediment. The equitability shows no noticeable changes as well, but a slight decrease is detected in the tephra layer (7, 8, 9 cm), which can be explained by a higher abundances of a few taxa like Parakiefferiella in that layer.

Ordination analysis

In order to distinguish the relationship between chironomid assemblages and environmental variables associated with the tephra layer, ordination analyses were performed. A preliminary Detrended Correspondence Analysis (DCA) pointed out that the gradient lengths are short (i.e. < 2 standard deviation units), indicating the usage of a linearµmodel (ter Braak & Prentice 1988). However, either a Principal Components Analysis (PCA) and a Redundancy Analysis (RDA) (as a direct gradient analysis) were performed using all the taxa and the two environmental variables that reflect the presence of the tephra layer: organicmatter (OM) and grain size (Phi). The first axis of the PCA analysis explained 29.5 % of the total variance of species data and, together, the first two axes explained 51.2 % of the total variance (Table 2). The RDA explained a lower percentage of the data than did the PCA; the first two axes of the RDA accounted for only 22.7 % of the total variance in the species data. The species-environment correlations for the RDA were 0.73 (axis 1) and 0.81 (axis 2) (Table 2). The statistical significance of the relationship between the taxa and the environmental variables was evaluated through a monte Carlo permutation test based on the RDA results. This analysis uses an F-ratio as a test statistic, which implies an F-value calculated from the data, denominated F0- by CANOCO, that is compared with a reference distribution. In contrast to other standard statistical tests where the reference distribution corresponds to the F-distribution, in theµmonte Carlo test, this reference distribution is actually determined from the data through the permutations (ter Braak & Smilauer 2002). In this case, 500 permutations were done for theµmonte Carlo test, which showed that the first canonical axis is not significant at the 1 % level (P = 0.056, Table 2) but, at the same time, indicated that all canonical axes are statistically significant at the 1 % level (P < 0.01, Table 2), suggesting a relationship between species and the given environmental variables.


Fig. 5 depicts a biplot diagram of the ordination; the thick lines represent the environmental variables and thin lines the species. It is possible to see that Tanytarsina type B, Eukiefferiella (Thienemann 1926), Pseudochironomus, Ablabesmyia, Parachirono-mus, Dicrotendipes, Tanytarsina type A, and Parakiefferiella are highly important in structuring the assemblage. The taxa Ablabesmyia, Parapsectrocladius (Cranston 2000), and Limnophyes seem to beµmore influenced by high grain size (Phi) and organicµmatter values, whereas CricotopuslOrthocladius, Djalmabatista, Chironomus (Meigen 1803), and especially Parakiefferiella appear to be sensitive to low Phi and organicµmatter values. It is important to clarify that Phi is a logarithmic scale of particle size in millimetres, whichµmeans high Phi values imply small particles. According to the ordination biplot, Parakiefferiella seems to prefer coarse grain over fine sediments.


Fig. 5: Ordination biplot of Chironomid taxon with thin arrows representing taxon and thick arrows for environmental variables (Phi and OM). Taxa key as follows: Ablab = Ablabesmyia, Eukieffe = Eukiefferiella, Chiro.u = Chironomini unidentified, Pseudoch = Pseudochironomus, Cory = Cory-noneura, Dicro = Dicrotendipes, Macrop = Macropelopia, Polyp = Polypedilum, Crico = Cricoto-pus, Phaen = Phaenopsectra, Parakie = Parakiefferiella, Chiron = Chironomus, Ortho.u = Orthocladiinae unidentified, Djal = Djalmabatista, Limno = Limnophyes, Tanyt.ta = Tanytarsini type A, Tanyt.tb = Tanytarsini type B, Parachi = Parachironomus, Tany.u = Tanypodinae unidentified, Parapsec = Parapsectrocladius.

Biplot del análisis de ordenación de los taxa de quironómidos representadas por flechas finas y las variables ambientales; tamañoµmedio (Phi) yµmaterial orgánica (OM), representadas por flechas gruesas. Abreviaciones como sigue: Ablab = Ablabesmyia, Eukieffe = Eukiefferiella, Chiro.u = Chironomini unidentified, Pseudoch = Pseudochironomus, Cory = Cory-noneura, Dicro = Dicrotendipes, Macrop = Macropelopia, Polyp = Polypedilum, Crico = Cricotopus, Phaen = Phaenopsectra, Parakie = Parakiefferiella, Chiron = Chironomus, Ortho.u = Orthocladiinae unidentified, Djal = Djalmabatista, Limno = Limnophyes, Tanyt.ta = Tanytarsini type A, Tanyt.tb = Tanytarsini type B, Parachi = Parachironomus, Tany.u = Tanypodinae unidentified, Parapsec = Parapsectrocladius.

DISCUSSION

Physical parameters

The tephra layer deposited between 7 and 12 cm in the sediment of Lake Galletué produced a marked change in the lake's sedimentological structure. In terms of sedimentological properties, the tephra layer has a low organic content, coarse grain size, and lower 210Pb content in comparison with the rest of the core. Considering its mean size (equivalent to sand), it was probably deposited in a short period of time (Telford et al. 2004).

According to the dating (210Pb, 137Cs), the sediment core covers the last ~70 years and the tephra deposition represents ca. 1957 AD. Some historical records of Andean volcanic activity (González-Ferran 1994) indicate that, in November 1956, an eruption of Llaima volcano, one of the biggest and most active in Chile (Moreno & Fuentealba 1994), produced lava fluxes, ash expulsion, and lahars (González-Ferran 1994). Moreno and Gardeweg (1989) described the eruption of Lonquimay volcano (December 1989), another recent volcanic event near Lake Galletué. This eruption expelled ash, lava, and other pyroclastic materials, causing serious damage to crops and cattle in the region (Besoaín et al. 1992). However, this eruption does not coincide with the tephra deposition established by 210Pb dating. Therefore, the tephra layer deposited in Lake Galletué between 7 and 12 cm was probably generated by the Llaima volcano eruption of 1957.

The 210Pb profile shows a general decreasing trend from the upper part of the core to lower levels. However, it is possible to observe lower activity in centimetres 2, 3, and 4 as compared to 1 and 5. Other studies have also reported a similar trend of 210Pb profiles in Chile, where activity does not always decrease constantly with sediment depth (Urrutia et al. 2000, Cisternas & Araneda 2001, Arnaud et al. 2006). Cisternas & Araneda (2001) attributed this reversal in activity to an increased sedimentation rate which, in turn, dilutes the 210Pb activity. Other causes of such an alteration include the mixing of sediments due to a seismic event or bioperturbation. In this short core from Lake Galletué, these two causes are discarded because the x-rays revealed a horizontal arrangement of the sediment layers and the visual inspection did not identify biological mixing. Thus, the reversal in the activity could be attributed to differences in the sedimentation rate of Lake Galletué.

Chironomids

Some studies in the northern hemisphere have indicated that volcanic eruptions and associated processes have the potential to cause significant impacts on human and natural ecosystems (Eastwood et al. 2002). Among the impacts that a volcanic event could induce in aquatic ecosystems are increased nutrient input due to chemical weathering of tephra and changes in physical conditions such as diminishing light penetration (short term) that seals the sediment-water interface or buriesµmacrophytes in littoral zones. Other impacts might include changes in the pH and salinity of the lake water (Birks & Lotter 1994, Heinrichs et al. 1999, Barker et al. 2000, Eastwood 2002).

These impacts, in turn, can produce changes in the organism assemblages living in the water column or sediment. Birks & Lotter (1994) reported changes in diatom assemblages after a tephra deposition near Laacher See Volcano, Germany. They found that diversity and accumulation rates of some taxa of both terrestrial vegetation and diatoms at the sites nearest the volcano were affected after tephra deposition. Hickman & Reasoner (1994), also working with diatoms but in British Columbia, found that tephra deposition affected diatom production, but could not find an effect on diatom diversity. Telford et al. (2004) described lacustrine responses to tephra falls, mainly represented in diatoms assemblages.

Regarding the effects caused by tephra on chironomids, Heinrichs et al. (1999) reported changes in assemblages at Kilpoola Lake (British Columbia) after the deposition of the mazama ash layer. Above the tephra layer, these authors found increased Cricotopusl Orthocladius abundance which, together with other characteristics of the assemblage, indicated increased salinity as a direct result of volcanic deposition. Tsukada (1967) also reported a decrease in Tanytarsus genuinus abundance after two events of volcanic sediment deposition in Lake Nojiri, Japan.

Massaferro & Corley (1998) used subfossil chironomid assemblages from Lakeµmascardi (41°20' S, 71°34' W) covering ca. 15 kyr BP to show that theµmost important factors affecting chironomid distribution in this lake are volcanism and climate cooling. They found sharp changes in chironomid diversity and equitability after the deposition of tephra layers that caused extreme conditions unsuitable for many species. Their results also indicate the complete absence of chironomid fauna within the tephra layers and a rapid recovery of diversity and equitability to their pre-disturbance levels once the tephra deposition had terminated.

Massaferro et al. (2005) found evidence of tephra impacts on chironomid fauna in Lakeµmorenito (41° S, 71° W). The abundance and diversity of chironomids decreased drastically along with organic content during episodes of volcanic sediment deposition. However, these authors pointed out that the most important fluctuation in chironomid assemblages was due to the anthropic disturbances of the watershed, reflected by the increased abundance of Chironomus, a typical inhabitant of mesotrophic and eutrophic environments. Human intervention in the lake by dam construction and a volcanic event in 1960 provoked increased diversity and the reappearance of Ablabesmyia, Paracladopelma, Phaenopsectra, and Dicrotendipes taxa. massaferro et al. (2005) suggest that the increase in Chironomus towards the upper part of the core and the decline of Tanytarsus gr., together with increased OM, could reflect more productive conditions within the lake. Nevertheless, they suggest that, due to the synchronicity of both the natural (1960 volcanic event) and anthropic (dam construction) impacts, it is difficult to track a direct cause and effect relationship for the changes in the chironomid assemblages.

Overall, our results from Lake Galletué indicate a decrease in the concentration of head capsules just after the tephra deposition, although this concentration increased later in the tephra layer. Within the tephra, Parakiefferiella increased noticeably, whereas Ablabesmyia fell in the same strata. The difference in abundance of these taxa indicates that the tephra deposition could have provided an advantage to Parakiefferiella in comparison with other taxon like Ablabesmyia, which was affected negatively. In the ordination biplot, Parakiefferiella is negatively correlated with high values of Phi and OM, suggesting that this taxon is more abundant in coarse grains and with low organicµmatter. Conversely, Ablabesmyia is positively correlated with both variables, probably beingµmore abundant with small grain sizes. Unfortunately, there is little ecological knowledge about chironomids in Chile that can help to interpret such changes, but some information generated elsewhere indicates that Parakiefferiella is a taxon typical of cold, well-oxygenated waters (Massaferro & Corley 1998, Porinchu & Cwynar 2002). Thus, the coarse (~ 300 µm up to 1 cm), highly porous tephra of Galletué could have maintained a higher oxygen level, more favourable to Parakieferiella.

There are others features of chironomid assemblages within the tephra layer. One is the slight increase of CricotopuslOrthocladius, which has low abundances both before and after the tephra layer. This behaviour coincides with the increment of the same taxon determined by Heinrichs et al. (1999) after a tephra deposition in British Columbia, associated with an increase in salinity due to volcanic sediment deposition. It is also possible to see the disappearance of Pseudochironomus and Corynoneura, and the appearance of Limnophyes, Chironomus, Phaenopsectra and Djalmabatista. On the other hand, after the tephra deposition, it is possible to see a slight recovery in some chironomid taxa, whichµmaintain low abundances during the tephra, like Ablabesmyia, Eukiefferiella, and Parachironomus. This suggests that the lake could have a resilience capacity currently tending to re-establish the conditions prevailing before the tephra deposition.

Although our results do not show a drastic change in chironomid diversity reflected in the Shannon index, the changes in the assemblages mentioned above no doubt indicated that tephra had an impact on the Lake Galletué chironomids. Previous investigations report changes in chironomid diversity during tephra depositions (Massaferro & Corley 1998, massaferro et al. 2005), and we suggest such differences could be explained by the characteristics of the tephra.

According to Lowe & Hunt (2001), the term "tephra" is a general term used for a broad range of sediments released from volcanic eruptions. Therefore, tephra characteristics vary greatly between different geographical zones or even between eruptions of the same volcano. The tephra of Lake Galletué is composed mainly of coarse particles (~300 µm up to 1 cm) with high porosity that seem to be favourable to Parakiefferiella. Although massaferro & Corley (1998) and massaferro et al. (2005) do not present a sedimentological characterization of the tephra layers identified in their profiles, it is possible that the tephra in Lakes mascardi and morenito have completely different characteristics than the tephra found in Lake Galletué. For example, volcanic sediment that is finer (less porous) orµmore soluble (changes in pH or salinity) could have had a different effect on the chironomid assemblages in Lake Galletué, which may have been reflected as changes in diversity.

Massaferro & Corley (1998) found that head capsules were completely absent in the tephra layer. In our results, we report a drop in the abundance of head capsules at the beginning of the tephra deposition but, shortly after, an increase all along the tephra layer.

According to Telford et al. (2004), the effects of tephra on aquatic biota are evident once the tephra is deposited because sedimentation of tephra particles (assuming an equivalent size to sand) is fast (~40µm h-1). These authors indicate that the presence of diatom remains within the tephra could be a result of sediment mixing processes. This statement also should be valid for our results, because we found chironomid remains within the tephra. The mixing of tephra particles with the host sediment is also evident at the beginning of tephra deposition (11 cm, Fig. 3). However, the tephra recorded in Lake Galletué is very coarse, with particles as large as 1 cm in diameter; thus, the high porosity could have allowed the percolation of fine sediments (S. Bertrand, unpublished data, 2004) and also the input of chironomids and diatoms (Cruces et al. 2006) towards the tephra layer.

CONCLUSIONS

The sedimentary record of Lake Galletué provides evidence of a 5-cm thick layer of volcanic sediment (tephra) deposited during a recent eruption near the watershed. The deposition of this tephra produced an interruption in the normal deposition of sediment, differing completely in mineralogical composition, organic content, and 210Pb activity from the host sediment. The geochronology established by 210Pb and 137Cs, along with the volcanic history of the area, indicate that this tephra deposition probably corresponds to the 1956-1957 eruption of the Llaima volcano.

This tephra deposition also generated changes in the aquatic biota assemblages, as reflected by diatoms. Our results also identified an impact on chironomid assemblages due to this deposition. The most noticeable change in the chironomid assemblage is the marked increase of Parakiefferiella within the tephra layer, and the decrease of Ablabesmyia in the same layer. After the tephra layer, a recovery was observed in the abundance of some taxa that were sensitive to the tephra deposition, suggesting that the lake has enough of a resilience capacity to restore the conditions prevailing before the impact.

On the other hand and contrary to our expectations, the tephra deposition did not produce a drastic change in the chironomid diversity index, as reported in other studies. We suggest that the properties of the tephra deposition (mineralogy, grain size, porosity, solubility) explain these different results.

 

ACKNOWLEDGEMENTS

This research was funded by projects Dirección de Investigación Universidad de Concepción (DIUC) numbers 204.310.039-1.0, 203.310.35-1.0, and by FONDECYT 1050647 and partially 1070508. Special thanks to A. Paggi for a warm reception in her lab during training in chironomid taxonomy; to I. Walker and S. Brooks for their help with taxonomical doubts; to C. Vivero for her valuable help with samples; and to E. Habit and R. Figueroa for help with statistical analysis. A.A. is grateful for a scholarship from Escuela de Graduados, Universidad de Concepción, and thanks Wallonia Community (Belgium) for funding a research stay and E. Chapron for his assistance in the fieldwork. Finally, this work would not have been possible without the loving support of my wife, Karina.

 

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Associate Editor: Claudio Latorre

Received May 19, 2006; accepted November 20, 2006

*e-mail for correspondence: aaraneda@udec.cl