Volcano

Nevado del Ruiz is the northernmost glacier-clad volcano of the Andean chain (Fig. 2). It is 5320m a.s.l. and is a composite stratovolcano with a flat summit and an ice cap. Arenas crater, with a diameter of 850m and a depth of 250 m, was the vent for the 13 November 1985 eruption. Like the neighbouring volcanoes of the Ruiz–Tolima massif, Nevado del Ruiz is topographically constrained by the Magdalena valley in the east and the Cauca valley in the west. Tectonically, Ruiz is located at the intersection of four faults, some of which are still active.

Fig. 2.

Schematic map of the Ruiz–Tolima volcanic area showing main drainages from the Nevados del Ruiz, Santa Isabel and Tolima volcanoes.

Ruiz is by far the best studied among Colombia’s glacier-clad volcanoes, due to the tragic disaster in 1985 that prompted a series of important studies. Many of these studies are collected in a special publication (Willliams, 1990a, b). The Quaternary and Holocene eruption history is fairly well known. Reference Thouret, Salinas and MurciaThouret and others (1990a) identified three main eruption periods in the 1.8 Ma long history of Nevado del Ruiz. At the end of the earliest period of activity, which was characterized by a partial collapse and formation of a caldera (∽1.0 to 0.8 Ma ago), a stratovolcano was built with deposits including massive pyroclastic density currents. The present edifice of the Ruiz volcano is a product of the activity over the last 150 000 years represented by a constructive phase featuring emplacement of a series of domes and thick lava flows of andesite and dacite magma.

During the last 11 000 years, 12 eruption stages, probably each with multiple eruptions, are identified. Processes included tephra fallout, pyroclastic density currents, multiple slope failures with debris avalanches and lahars, and interaction with the ice cap (Reference Thouret, Salinas and MurciaThouret and others, 1990a). Debris avalanches and lahars particularly affected the Azufrado and Lagunillas rivers. Three historic events are recorded: 1595, 1845 and 1985. The 1595 event was characterized by explosive eruptions and debris avalanches transforming into lahars (Reference Pierson, Janda, Thouret and BorreroPierson and others, 1990). In 1845, a small phreato-magmatic eruption took place, claiming 1000 lives as populated areas were inundated in a similar but more extensive way as in 1985. In terms of lahar volumes, the 1845 event was the largest (about 300× 10⁶m³ of total lahar volume), followed by the 1595 and the 1985 lahars (Reference Thouret, Cantagrel, Salinas and MurciaThouret and others, 1990b). Since 1985, fumarolic activity has been continuously observed at the Arenas crater, and various hot spring locations were detected around the volcano.

Glaciers

The ice cap on Nevado del Ruiz can be divided into about eight drainage basins and corresponding outlet glaciers. Lagunillas, Recio and Guali-Molinos glaciers, which drain to the corresponding river systems, comprise most of the ice mass. The ice cap has been strongly affected by glacier retreat in recent decades, with glacier area reduced by more than 50% in the last 40 years (Fig. 3). Estimates of the pre-and post-1985 eruption glacier area vary between 19– 25 km² and 17–21km², respectively (Reference ThouretThouret, 1990; Reference CeballosCeballos and others, 2006). During the two decades following 1985, there has been another 40–50% loss of the glacier area with measurements from 2002 and 2003 showing an area of only 10.3 km² (Table 1). Ground penetrating radar studies performed in 1999 revealed a maximum ice thickness of 190m with an average thickness of 47m (Reference CeballosCeballos and others, 2006). Taking into consideration that the glacier has been continually thinning since 1999, an upper estimate for the total ice volume of 484×10⁶m³ can be derived for 2003. Based on an average ice density of 0.85 g cm^–3 (including the top snow and firn layers), a water equivalent of 411×10⁶m³ is calculated. Single glacier tongues that reached elevations of 4500–4600m a.s.l. in 1986 have now retreated to 4800–4900m a.s.l. Also, erosion by pyroclastic density currents generated by the 1985 eruption significantly reduced the size of several outlet glaciers, in particular those of Lagunillas and Azufrado glaciers (Fig. 3). These glaciers have remained in a fractured, unstable state since the eruption but no significant ice avalanches have been observed.

Fig. 3.

Reduction of glacier surface area in recent decades for the four glacier-capped volcanoes in Colombia. Note acceleration in retreat rates since the mid-1980s for Nevado del Ruiz, related to the 1985 eruption.

Interactions and hazards

Interactions between volcanic activity and the ice caps are the key to the Ruiz paradox, which is that a small eruption could lead to one of the world’s largest volcanic disasters in history. Based on the extensive studies related to the 1985 disaster, processes and associated hazards of volcano–ice interactions can be readily assessed for Nevado del Ruiz. The main processes identified are: pyroclastic density currents that are able to generate large amounts of meltwater if hot debris is mechanically mixed with snow and ice (Reference Pierson, Janda, Thouret and BorreroPierson and others, 1990; Reference WalderWalder, 2000); slush avalanches induced by sudden loading of snow and firn on steep and unstable slopes (Reference ThouretThouret, 1990); and rock and ice avalanches triggered by seismic shaking, percolating meltwater and sudden increase of shear stress due to overriding pyroclastic density currents (Reference Pierson, Janda, Thouret and BorreroPierson and others, 1990; Fig. 1). The low density and cohesion of snow facilitate easy scouring and entrainment, and were probably responsible for generating much of the 1985 meltwater (Reference ThouretThouret, 1990). Dilute flows and avalanches rapidly transformed into debris flows in the river channels by entrainment of sediment. The total volume of lahars reaching downstream areas was about 90×10⁶m³, mean peak velocities ranged from 5–15ms^–1, and a peak discharge of 48 000m³ s^–1 was reached in the Azufrado valley 9 km from the source (Reference Pierson, Janda, Thouret and BorreroPierson and others, 1990). The river systems mainly affected by lahars were the Lagunillas, Azufrado and Guali in the east to northeast, and Nereidas/Molinos in the west. The travel time of lahars, an important consideration for early warning, was slightly more than one hour for the first 50 km (Azufrado). Armero was reached in little over 2 hours while the most distant areas affected by lahars, more than 100 km away from the source, were reached in about 4 hours.

The Holocene eruption history of Ruiz provides evidence that lahars are common phenomena and the most serious and far-reaching hazard (Reference Thouret, Cantagrel, Salinas and MurciaThouret and others, 1990b). Lahar volumes ranged from about 90 (1985) to 300 (1845) million m³. The volume of the 1595 eruption-related lahars is intermediate but not exactly known (Reference HerdHerd, 1982; Reference Pierson, Janda, Thouret and BorreroPierson and others, 1990). In addition to meltwater-induced lahars generated by the interaction of snow and ice with hot eruption products, floods from water stored within the ice or along the river channels require consideration. The lahars in 1845, for example, were probably enlarged by a flood released from the breaching of a dam formed by a contemporaneous debris avalanche (Reference Thouret, Cantagrel, Salinas and MurciaThouret and others, 1990b).

It is estimated that about 10% of the ice volume was removed during the 1985 event (Reference Pierson, Janda, Thouret and BorreroPierson and others, 1990; Reference ThouretThouret, 1990). Since then, the glaciers have significantly retreated. The reduced area and the decreased mass of ice lying on steep topography suggest that an eruption similar in magnitude to that of 1985 (VEI = 3) would not mobilize more than 10% of the present ice volume. A larger eruption, however, could easily interact with a greater ice volume. Under present conditions, a 10% water equivalent of the total ice mass on Ruiz would amount to ∽40×10⁶m³ of water. For an estimate of the combined lahar volume we assume that 30% of this water would not be directly available for lahar generation (water trapped and diluted in the ice and sediment; Reference ThouretThouret, 1990). For the 1985 lahars, the water concentration (by volume) of the initial lahars was estimated to be 0.6–0.8 (Reference Pierson, Janda, Thouret and BorreroPierson and others, 1990). The initial lahar volume for present conditions would therefore be 35–47×10⁶m³. Based on bulking factors of 2–4 observed in 1985 (Reference Pierson, Janda, Thouret and BorreroPierson and others, 1990), we estimate the combined lahar volume to reach distal deposition zones to be 70–188×10⁶m³ (Table 1). This means that the magnitude of lahars could be similar to those in 1985, but could also be larger in spite of the reduced ice volume. This is not necessarily an inconsistency because the critical processes determining the final lahar volume (i.e. eruption magnitude, formation of initial lahars and bulking factors) have some range of variation and could be more vigorous than those observed in 1985, as other case studies have shown (e.g. Reference Scott, Vallance, Kerle, Macías, Strauch and DevoliScott and others, 2005). The range of potential lahar volumes indicates that downstream areas would consequently be severely affected again.

In addition to hazards related to eruption activity, non-eruption processes must be taken into consideration, including rock/ice avalanches due to earthquakes and flank failures, particularly in the northeast Azufrado sector where evidence exists for multiple flank failures (Reference Thouret, Cantagrel, Salinas and MurciaThouret and others, 1990b; Fig. 1). Further details on current conditions and hazards on Nevado del Ruiz are provided by Reference ThouretThouret and others (2007).

Volcano

Nevado de Santa Isabel is the third highest volcano (4965m a.s.l.) on the Pliocene to early Pleistocene Ruiz–Tolima plateau (1500km²). It is located 10km south of Nevado del Ruiz and 18km north of Nevado del Tolima (Fig. 2). Unlike its two neighbouring volcanoes, Nevado de Santa Isabel does not have a plateau ice cap; it is rather constructed as a north–south trending ridge with a number of domes and two main peaks. It is drained by the rivers Otún and Claro to the west and Totarito towards the Magdalena valley in the east. The volcanic history of Nevado de Santa Isabel is not as well known than that of its neighbours. Three domes named Norte (north), Centro (centre) and Sur (south), of Pleistocene age and andesite composition, were identified in the summit area. No historic activity is known to date but lava flows originating from the aforementioned domes with the same age and composition were found. More recent blocky lavas were dated 2800, 5500, 6750 and 7450 years BP (Reference MéndezMéndez, 1997). In the summit area beneath the lava flows, there are pyroclastic density current deposits from the northern dome that consist of ash and pumice. The main eruption products are restricted to a distance of 5–8 km from the summit.

Table 1.

Glacier surface areas, estimated ice volumes and derived potential lahar characteristics of the ice-capped volcanoes in the Cordillera Central in Colombia

Glaciers

In 2002, the ice mass on Nevado de Santa Isabel extended over an area of 3.3 km² and could be divided into 19 different drainage basins each terminating in small outlet glaciers. According to ground penetrating radar profiles taken in north–south and east–west directions in 2000, the maximum ice thickness in the summit region is 103 m. Towards the ice margin, values range from ∽20–80 m. Taking an average thickness of 60 m, we calculate a total ice volume of 198×10⁶m³, which is equivalent to 168× 10⁶m³ of water (based on an average ice density of 0.85 g cm^–3) (Table 1). Ice volume estimates made by Reference LinderLinder (1991) for 1987 were considerably lower but no direct ice thickness measurements were available at that time. Glacier fluctuations on Nevado de Santa Isabel have been monitored regularly during the last 15–17 years. During this period, the steady retreat of outlet glaciers has been recorded almost on an annual basis. Measurements of the ice surface area go back to 1946 and are based on aerial photographs and more recently on satellite images. In the last decades the glaciers on Nevado de Santa Isabel have, in fact, experienced one of the most dramatic shrinkages of any glaciers in Colombia. Since 1850 (ice surface reconstructed according to the position of Little Ice Age moraines) the glaciers have been reduced by almost 90% in terms of area. The retreat rate has accelerated in the last few decades; in <20 years the area covered by glaciers has been reduced by about 50% (Reference CeballosCeballos and others, 2006; Fig. 3). In the same period, glacier margins retreated by as much as 250 m.

The observed rise of the equilibrium line altitude (ELA) on Nevado del Santa Isabel is about 190 ±30 m for the period 1850 to 2002 and 95±30m for 1959 to 2002 (Reference BaumannBaumann, 2006). If this rise in ELA resulted only from elevation of surface temperature, the corresponding temperature rise would be 1.2 ±0.28C and 0.6 ±0.28C for 1850 to 2002 and 1959 to 2002, respectively (with a lapse rate of 0.658C per 100 m), implying an accelerated rate of ELA rise over the last 40 years by a factor of ∽2. A direct comparison with measured temperature changes is difficult since high-mountain temperature records, in particular long-term, are generally rare throughout Colombia. One of the few meteorological stations (Las Brisas) is located 12 km north of Nevado de Santa Isabel and 5 km from Nevado del Ruiz at 4150m a.s.l. Measurements from the mid-1980s to mid-1990s indicate a temperature rise of about 0.58C. Another station in the Sierra Nevada del Cocuy in northeast Colombia at 3716m a.s.l. shows an increase in temperature of about 18C from 1974 to 2000. Application of a simple parameterization scheme assuming a step-wise change in mass balance (Reference Haeberli and HoelzleHaeberli and Hoelzle, 1995) and a mass balance gradient of 1.9m per 100 m results in a mass balance deficit of 0.4–0.6ma^–1 water equivalent for 1959 to 2002.

Interactions and hazards

The past eruption activity of Nevado de Santa Isabel has been predominantly effusive. Heat transfer through the bases and sides of lava flows is generally not efficient enough to melt the amount of snow and ice required to generate lahars or floods (Reference Major and NewhallMajor and Newhall, 1989). Snow and ice melted by subaerial lava flows is usually converted to steam. The process of steam production without generation of any significant lahar has been observed on Llaima and Villarica volcanoes in Chile in 1979 and 1984, respectively (Reference Moreno, Gonzales-Ferran and RiffoMoreno and others, 1981; Reference Gonzalez-FerranGonzalez-Ferran, 1985). On both volcanoes, small mixed rock and ice avalanches were produced as the lava flow chilled, fragmented and mixed debris with snow and ice (Fig. 1). Llaima and Villarica volcanoes, however, have a much larger ice cover than Nevado de Santa Isabel where lava flows can only travel a maximum distance of 500–700m on snow and ice. Therefore, generation of significant avalanches or meltwater by advancing lava flows is unlikely on Nevado de Santa Isabel. Pyroclastic density currents are far more effective at melting ice and snow than lava flows. At Nevado de Santa Isabel, pyroclastic density currents could result from collapse of domes or lava flows. In the past, however, pyroclastic density currents have been documented as rare occurrences, and had a limited reach of only 5 km from the vent. Dome collapse could also involve avalanches, which would probably entrain ice and snow.

At present, there is no indication of renewed activity at Nevado de Santa Isabel, and therefore eruption-induced hazards are not likely in the near future. A more likely scenario involves lahars resulting from snow/ice melt events generated by rainstorms sufficiently large to mobilize ash and other unconsolidated sediment to form a debris flow. In view of the rare occurrence of such mass movements in historic times, the massive retreat of glaciers on Nevado de Santa Isabel in recent decades and the existence of attenuation zones in the run-out of the stream channels before reaching populated areas, we consider that there is only a limited hazard of a major lahar with potential for downstream destruction. Furthermore, we have no indication of an increased thermal heat flux on Nevado de Santa Isabel that could cause melting at the base of the glacier and induce glacier instabilities.

Volcano

Nevado del Tolima is part of the basaltic andesite and andesite Ruiz–Tolima volcanic massif, but is offset 15 km to the southeast from the main volcanic range. The 5280m a.s.l. Tolima is composed of a cluster of lava domes and extrusions nested in an inferred summit caldera of late Pleistocene age (Reference Thouret, Cantagrel, Robin, Murcia, Salinas and CepedaThouret and others, 1995). The lava domes are underlain by a dissected stratovolcano. Holocene glacial deposits and products from pyroclastic density currents form the top of the mountain. Four major valley systems drain Nevado del Tolima: Rio Totaré (north), Rio San Rumualdo (east), Rio Combeima (south) and Rio Toche (west) (Fig. 2). Due to the offset from the main mountain range, all these rivers eventually drain to the Rio Magdalena valley in the east. The closest and most populated settlements are located along the Rio Combeima, with the provincial capital of Ibagué (∽400 000 inhabitants) situated 27 km from the summit of Nevado del Tolima.

Reference Thouret, Cantagrel, Robin, Murcia, Salinas and CepedaThouret and others (1995) distinguished four major sequences of edifice growth and destruction during the past 1.4 Ma. A caldera collapse occurred in late Pleistocene times. From 16 000 years BP, several eruption stages with explosive characteristics have been recorded, e.g. a violent crater opening between 16 200 and 14 000 years BP, a large plinian eruption between 13 000 and 12 300 years BP and another smaller plinian eruption ∽3600 years BP. Several deposits of pyroclastic density currents in the late and middle Holocene are known, with some indicating probable interactions of magma and ice. The total volume of pyroclastic deposits from the Holocene is estimated to be ∽2.5 km³ (Reference Thouret, Cantagrel, Robin, Murcia, Salinas and CepedaThouret and others, 1995). During this time, small-volume rock falls also occurred, destroying part of the northeast flank of the summit. In late pre-historical and historical times, only eruptions of moderate size (VEI 2–3) have taken place. Activity was recorded a few times in the 18th and 19th centuries, the last in 1943 (VEI 2). The remoteness of the volcano and limited visibility due to convective tropical cloud coverage are, however, the main reasons for the lack of detailed documentation of these events (Reference KruegerKrueger, 1927; Reference KrausKraus, 1944). Predominantly fumarolic activity has been observed in the last few decades, concentrated on the southwest area of the crater (Reference Cepeda, Murcia, Thouret and RossiCepeda and others, 1988). The existence of hot springs on the northeast and southern slopes, and weak seismicity captured by INGEOMINAS (Instituto Colombiano de Geología y Minería) seismic stations, are further signs of current volcanic unrest.

Glaciers

The ice cap on Nevado del Tolima extends into four main glacial basins draining the above-mentioned rivers (Fig. 4). The extent of the ice cap at the end of the last Ice Age (14 000–12 000 years BP) was in the range of 35 km² (Reference Thouret, Cantagrel, Robin, Murcia, Salinas and CepedaThouret and others, 1995). Volcanic eruptions during this period likely involved significant magma–ice interactions. At the end of the Little Ice Age (∽1850), the ice extent had decreased to 8.6 km² with terminus positions no lower than 4300m a.s.l. The last 150 years, on Nevado del Tolima as elsewhere, have been characterized by rapid ice retreat: from 2.7km² in 1958, to 1.6km² in 1987, to 1.2 km² in 1997 and eventually 1.04 km² in 2002 (Fig. 3).

Ground penetrating radar measurements in 1998 found a maximum ice thickness of 175 m and an average thickness of 70m yielding an estimated total ice volume of 73× 10⁶m³. Assuming an average ice density of 0.85 g cm^–3, a water equivalent of 62×10⁶m³ can be derived. The large ice thickness is remarkable in view of the small ice surface area and is related to the crater morphology of the summit, which facilitates ice accumulation. The ice quickly thins from the massive ice cap towards the heavily crevassed outlet glaciers (Fig. 4). Ongoing atmospheric warming will continue to affect the outlet glaciers with further reduction in ice extent. The related impact on the summit ice cap will result in a reduction of ice thickness. However, due to the large thickness, ice will remain much longer on Nevado del Tolima than what the small area of 1 km² and linear extrapolation of glacier area reduction would suggest.

Fig. 4.

The ice cap of Nevado del Tolima with Combeima outlet glacier. The steep slopes with strongly fractured ice and unstable rock faces are clearly visible.

Interactions and hazards

The past extent of the ice cap on Nevado del Tolima makes the occurrence of volcano–ice interactions a very likely scenario for eruption activity in the late Pleistocene and Holocene. Based on the geological record and the current conditions, the most important volcano–ice processes in terms of hazards are the generation of large debris flows due to scouring and melting of ice by pyroclastic density currents, and ice and rock avalanches which can also be transformed into more mobile debris flows.

The likelihood of future eruptions may be seen in view of the average occurrence interval of 2000–4000 years between major eruptions and the current period of about 1700–3600 years since the last major eruption. A future eruption may well be of explosive character as suggested by the explosive history of the volcano and the magmatic evolution (dacite and andesite) observed in the Holocene eruption products (Reference Thouret, Cantagrel, Robin, Murcia, Salinas and CepedaThouret and others, 1995).

In spite of the rapid reduction in ice surface area in the past decades, a large volume of ice remains on the summit of Nevado del Tolima. A 10% melting of the ice volume (as was the case during the 1985 Nevado del Ruiz eruption) could produce an initial lahar volume of 5.4–7.2×10⁶m³, based on a 70% availability of meltwater and an initial water concentration of 0.6–0.8. Total combined lahar volumes reaching downstream areas could then be 11– 29×10⁶m³ (based on downstream bulking rates of 2 to 4) (Table 1). Lahar volume could additionally be enhanced by water input from precipitation, tributary rivers and melt from seasonal snow cover. Although Rio Toche and Rio Totare have rather low gradients, there is substantial potential for bulking because of the presence of unconsolidated deposits of pumice and ash. In these river systems, deposits from mid-Holocene lahars of 6–10m thickness were found as far away as 60–70km from the source (Reference Thouret, Cantagrel, Robin, Murcia, Salinas and CepedaThouret and others, 1995). Medium-magnitude lahars would probably attenuate by energy dissipation in the flat sections of the streams.

The topography of the Rio Combeima catchment, which drains 60% of the total ice surface, is characterized by a steep and deep valley, and hence lahars would bulk more quickly and travel at higher speeds. The city of Ibagué, located along Rio Combeima at a distance of 27km and a vertical drop of 3600 m from the Nevado del Tolima summit, could be reached by lahars in about 40–60 min (Reference Cepeda, Murcia, Thouret and RossiCepeda and others, 1988; Reference Thouret, Cantagrel, Robin, Murcia, Salinas and CepedaThouret and others, 1995) while the upstream settlement of Juntas could be reached in less than 30 min. The fact that Ibagué is built on lahar deposits confirms the vulnerability of the city to high-magnitude lahars from Nevado del Tolima.

An additional hazard on Nevado del Tolima stems from ice and rock avalanches. Factors that contribute to these types of mass movement are the strongly crevassed structure and the steep slope gradient of the outlet glaciers. An eruption of VEI ≥3 could trigger major ice–rock avalanches by pyroclastic current impact and eruption seismicity, which subsequently could transform into more mobile debris flows (Reference Scott, Macías, Naranjo, Rodriguez and McGeehinScott and others, 2001) and affect the downstream communities of the Combeima catchment.

Ice–rock avalanches can also occur in times of no eruptions. The region is seismically highly active, and consequently earthquakes could effectively destabilize the glaciers on Nevado del Tolima. Furthermore, geothermal heat flow or fumarolic activity could lead to an increased melt at the ice–bedrock interface and thus reduce resistance forces, eventually resulting to failure. Similar processes are thought to be responsible for the high frequency of ice–rock avalanches of up to 30×10⁶m³ on Iliamna volcano, Alaska (Reference Caplan-Auerbach and HuggelCaplan-Auerbach and Huggel, 2007).

Volcano

Nevado del Huila is the southernmost glacier-clad volcano of Colombia’s Cordillera Central. Remoteness, topography and guerrilla activity make access difficult, which is the main reason why there are few studies of this volcano. Our understanding of the formation and history of Nevado del Huila thus remains limited, but recent investigations have yielded new information (Reference Pulgarín, Correa, Cepeda and AncocheaPulgarín and others, 2001). Nevado del Huila is a stratovolcano and located at the intersection of the states of Cauca, Huila and Tolima. The plan-view shape of the volcano is elliptical, with major and minor axes of 16 and 11 km, respectively. The maximum elevation is 5365 m a.s.l. There is no clear evidence of a crater; instead the peaks named Norte, Cresta, Central and Sur form the top of the edifice. The drainage system of Nevado del Huila is somewhat peculiar since the main rivers Páez and Símbola both drain to the south (Fig. 5). The Nevado del Huila volcanic complex was formed by two edifices, the older one (Pre-Huila) with a series of andesitic lavas that extended up to 15 km. During the period of the current edifice (Huila) andesitic to dacitic lavas were produced, along with small pyroclastic density currents generated by collapse or explosion of domes. The most recent volcanic products were characterized by a higher viscosity. It is notable that in the late Pleistocene the volcano suffered a partial collapse of the southern flank causing a major debris avalanche with an estimated volume of 5.4 km³ and covering an area of 36 km² down the Páez river (Reference PulgarínPulgarín, 2003). The flank collapse was facilitated by the reduced strength of hydrothermally altered material.

Fig. 5.

Schematic map of the Nevado del Huila and the main drainage of the Páez river. Also shown is the distribution of volcanic formations and the prehistoric debris avalanche deposits. Geologic time scale: Q: Quaternary; Q–Upper Ng: Quaternary to Upper Neogene; Mz: Mesozoic.

Nevado del Huila has had no recorded eruption activity in historic times. Fumarolic activity, however, has been known for the last 400 years, mainly on the glaciated area of the Central and Norte peaks. Hot springs are observed at the western flank of the volcano at the limit of Nevadas glacier and further downstream from El Mayor glacier. Seismic activity has been recorded since 1986, with a continuous record since 1993 at the INGEOMINAS volcano observatory in Popayán. Seismic events of volcanic–tectonic origin with magnitude less than 2.5 take place along a southwest–northeast trend. Earthquakes occur at depth (up to 8 km) and more superficially (less than 5 km) in the upper part of the edifice. The seismic network currently consists of four stations, of which two are located within 3 km of the summit, close to the glacier terminus.

Glaciers

The ice mass on Nevado del Huila is developed on four peaks along a north–south extension with glacier tongues descending towards the west and east (Fig. 6). The glaciers, in particular towards the termini, are steeply inclined and highly crevassed. Those tongues extending furthest downstream (El Mayor, El Oso and El Venado) reached an altitude between 4160 and 4430m a.s.l. in 1995. In general, the glaciers on Nevado del Huila are relatively unstudied. Reference Pulgarín, Jordan and LinderPulgarín and others (1996) provided the most important information in terms of geometry, extent and recent changes. The reduction of the glaciated area between 1960 and 2000 was ∽25% (Reference CeballosCeballos and others, 2006). The area decreased from 13.9 km² in 1990 to 13.3 km² in 1995 and 12.95 km² in 2001 (Fig. 3). The glacier tongues receded comparatively moderately; El Mayor, for instance, from 4053m a.s.l. in 1961 to 4163 m a.s.l. in 1995 and El Oso from 4040 m a.s.l. to 4432 m a.s.l. in the same period.

Fig. 6.

Map of the ice cap on Nevado del Huila. The glacier outlines correspond to ice extents in 1961, 1989 and 1995 (white lines). Circles indicate areas of fumarolic activity. Outlet glaciers exposed to the north, west and south feed Rio Páez; those exposed to the east feed Rio Símbola.

Ice thicknesses have not been measured on Huila but if we assume a similar average ice thickness as on Nevado del Ruiz (50 m), the 2001 ice volume can be estimated at 648×10⁶m³ (550×10⁶m³ water equivalent based on a density of 0.85 g cm^–3). Thinning of the ice thickness, however, has been measured for the last 45 years. Average annual thinning during this period has been 0.43 m, with a total average annual loss of ice of ∽10×10⁶m³ and an increasing rate of loss in more recent years (Reference Pulgarín, Jordan and LinderPulgarín and others, 1996). A crude linear extrapolation of this trend would doom glaciers on Nevado del Huila to extinction around 2070.

Interactions and hazards

The geologic and historic record highlights debris avalanches and related debris flows as a serious potential hazard. Most notable was the 1994 event in which a magnitude 6.4 earthquake triggered a large number of landslides (∽3000) and small debris avalanches which coalesced into a debris flow that descended the Páez river at inundation heights of 40m and maximum velocities of 25ms^–1. It caused the death of about 1000 people and massive damage (Reference Scott, Macías, Naranjo, Rodriguez and McGeehinScott and others, 2001; Reference PulgarínPulgarín, 2003; Fig. 7). Although this catastrophe was not related to volcano–ice interactions, we suggest that it draws a realistic picture of hazards with triggering mechanisms that could well originate at the ice-covered areas of Nevado del Huila.

Fig. 7.

Effects of the 1994 debris flow from Nevado del Huila in the Páez river at the town of Belalcázar, where flow heights reached over 20 m. Trimlines of the 1994 flow are indicated. (Photograph courtesy of H. Cepeda.)

Several factors affect the evaluation of potential volcanogenic hazards on Nevado del Huila. The volcanic history is poorly known and characteristic magnitude and periods of eruption are thus difficult to assess. The tendency towards higher magma viscosity of the most recent volcanic products and identification in the mid-1990s of pyroclastic deposits (Pulgarín and Correa, 1997) suggest that explosive activity cannot be excluded in the future. The large ice mass on Nevado del Huila bears a very significant amount of water (equivalent) potentially available for generation of mass flows. Steep topography, the fractured ice structure, high seismicity and potential geothermally induced melting at the ice–bedrock interface render the glaciers prone to instability. Several zones of hydrothermally altered rock enhance the potential for slope failure. Consequently, as the 1994 disaster showed, the population along the Páez river is highly vulnerable. High-magnitude mass movements could furthermore affect the Betania reservoir dam (used for hydropower generation) at a distance of more than 150 km from the source areas (Table 1).