Laguna del Maule (volcano)

Laguna del Maule is a volcanic field in the Andes mountain range of Chile, close to, and partly overlapping, the Argentina–Chile border. The bulk of the volcanic field is in the Talca Province of Chile's Maule Region. It is a segment of the Southern Volcanic Zone, part of the Andean Volcanic Belt. The volcanic field covers an area of 500 km2 and features at least 130 volcanic vents. Volcanic activity has generated cones, lava domes, lava coulees and lava flows, which surround the Laguna del Maule lake. The field gets its name from the lake, which is also the source of the Maule River.

The field's volcanic activity began 1.5million years ago during the Pleistocene; such activity has continued into the postglacial and Holocene era after glaciers retreated from the area. Postglacial volcanic activity has included eruptions with simultaneous explosive and effusive components, as well as eruptions with only one component. In the postglacial era, volcanic activity has increased at Laguna del Maule, with the volcanic field rapidly inflating during the Holocene. Three major caldera-forming eruptions took place in the volcanic field prior to the last glacial period. The most recent eruptions in the volcanic field took place 2,500 ± 700, 1,400 ± 600 and 800 ± 600 years ago and generated lava flows; today geothermal phenomena occur at Laguna del Maule. Volcanic rocks in the field include basalt, andesite, dacite and rhyolite; the latter along with rhyodacite makes up most of the Holocene rocks. In pre-Columbian times, the field was a regionally important source of obsidian.

Between 2004 and 2007, ground inflation began in the volcanic field, indicating the intrusion of a sill beneath it. The rate of inflation is faster than those measured on other inflating volcanoes such as Uturunku in Bolivia and Yellowstone Caldera in the United States and has been accompanied by anomalies in soil gas emission and seismic activity. This pattern has created concern about the potential for impending large-scale eruptive activity.

Geography and structure
The Laguna del Maule volcanic field straddles the Chilean–Argentine frontier; most of the complex lies on the Chilean side. The locality belongs to the Maule Region, of Talca Province in the Andes mountain range; it is close to the confluence of the Maule and Campanario rivers in the Maule valley. The city of Talca lies about 150 km west. The Argentine section of the field is in the Mendoza and Neuquén provinces, and the city of Malargüe is located about 140 km east from the volcanic field. Highway 115 (Chile) passes through the northern part of the volcanic field, and the Paso Pehuenche mountain pass is a few kilometres northeast of the lake; the region is otherwise sparsely inhabited and economic activity is limited to oil prospecting, pastures and tourism.

The Laguna del Maule volcanic field covers a surface area of 500 km2 and contains at least 130volcanic vents including cones, lava domes, lava flows, and shield volcanoes; 36silicic coulees and lava domes surround the lake. Over 100 km2 of the field is covered by these volcanic rocks. The volcanic field lies at an average height of 2400 m, and some summits around Laguna del Maule reach altitudes of 3900 m. Volcanic ash and pumice produced by the eruptions has been found over 20 km away in Argentina. A number of Quaternary volcanic systems of various ages surround Laguna del Maule lake, including about 14 shield volcanoes and stratovolcanoes that have been degraded by glaciation.

Among the structures in the volcanic field, the Domo del Maule lava dome is of rhyolitic composition and generated a lava flow to the north that dammed the Laguna del Maule. This lava flow is joined by other lava flows from the Crater Negro, a small cone in the southwest sector of the volcanic field; the lavas of this cone are andesitic and basaltic. Loma de Los Espejos is a large lava flow of acidic rocks that is 4 km long in the northern sector of the volcanic field, close to the outlet of Laguna del Maule. It consists of two lobes with a volume of about 0.82 km3 and contains obsidian and vitrophyre. Crystals within the flow reflect the sunlight. The well-preserved Colada de las Nieblas lava flow is in the extreme southwest sector of the volcanic field and originates at a tuff cone. This lava flow is 300 m thick, varying from 5 km to 6 km in length, and is about 3 km wide. The Barrancas centre has a volume of 5.5 km3 and reaches an elevation of 3092 m.

Past glaciation of this part of the Andes left traces in adjacent valleys, such as their U-shaped or trench-shaped outline. The older volcanics of Laguna del Maule have been disproportionately eroded by glacial action. Slopes around Laguna del Maule lake are covered by colluvium including talus.

The Laguna del Maule lake lies on the crest of the Andes, within a depression with a diameter of 20 km. The lake has a depth of 50 m and covers a surface of 54 km2; the surface is at an altitude of 2160 m. The name of the volcanic field comes from the lake; the Maule river originates there and the Barrancas River has its headwaters in the volcanic field as well. Terraces around the lake indicate that water levels have fluctuated in the past; the lake is regulated by a dam at the outlet that was built in 1950 and completed in 1957. An eruption dated between 19,000 ± 700 and 23,300 ± 400 years ago dammed the lake 200 m higher than its present level. When the dam broke 9,400years ago, a lake outburst flood occurred that released 12 km3 of water and left traces, such as scour, in the down-valley gorge. Benches and beach bars developed on the lake, which has left a shoreline around Laguna del Maule lake. Additionally, tephra fallout such as from the 1932 Quizapu eruption has impacted the lake through the Holocene and affected life in the lake waters.

Besides Laguna del Maule, other lakes in the field are Laguna El Piojo on the Chilean side in the southwest sector of the field, Laguna Cari Launa on the Chilean side in the northeastern sector of the field, and Laguna Fea in the south at 2492 m elevation and Laguna Negra lake both on the Argentine side. The Laguna Sin Salida ("lake without exit"; so named because it lacks a river running out of it) is in the northeastern sector of the volcanic field and it formed within a glacial cirque.

Geology
Subduction of the eastern part of Nazca plate beneath the western margin of the South America Plate occurs at a rate of about 74 ±. This subduction process is responsible for growth of the Chilean Andes, and volcanic and geothermal manifestations such as the 1960 Valdivia earthquake and the 2010 Chile earthquake, as well as Laguna del Maule, which formed 25 km behind the volcanic arc.

A phase of strong volcanic activity began in the Andes 25million years ago, probably due to increased convergence rates of the Nazca and South America plates for the past 28million years. It is likely that this phase persisted without interruption until today.

The subduction of the Nazca plate beneath the South America plate has formed a volcanic arc about 4000 km long, which is subdivided into several segments distinguished by varying angles of subduction. The part of the volcanic belt named the Southern Volcanic Zone contains at least 60volcanoes with historical activity and three major caldera systems. Major volcanoes of the Southern Volcanic Zone include from north to south: Maipo, Cerro Azul, Calabozos, Tatara-San Pedro, Laguna del Maule, Antuco, Villarrica, Puyehue-Cordon Caulle, Osorno, and Chaiten. Laguna del Maule is located within a segment known as the Transitional Southern Volcanic Zone, 330 km west of the Peru–Chile Trench. Volcanoes in this segment are typically located on basement blocks that have been uplifted between extensional basins.

In the area of Laguna del Maule, the subducting Nazca plate reaches a depth of 130 km and is 37million years old. During the Late Miocene, the convergence rate was higher than today and the Malargüe fold belt formed east of the main chain in response. The Moho is found at depths of 40 - 50 km beneath the volcanic field.

Local
The Campanario Formation is 15.3 to 7million years old and forms much of the basement in the Laguna del Maule area; this geological formation contains andesitic-dacitic ignimbrites and tuffs with later dacitic dykes that were emplaced 3.6–2.0 million years ago. An older unit, of Jurassic–Cretaceous age, crops out northwest of the volcanic field. Other units include an Oligocene–Miocene group of lacustrine and fluvial formations named Cura-Mallín, and another intermediary formation named Trapa-Trapa, which is of volcanic origin and between 19and 10million years old. Remnants of Quaternary ignimbrites and Pliocene, early Quaternary volcanic centres, are also found around the field; they form the Cola del Zorro Formation, which is partly covered by the eruption products of Laguna del Maule. Glacial tills occur at the volcanic field.

Faults such as the Troncoso Fault lie within the southwest sector of the volcanic field. Troncoso is alternatively described as a strike-slip or as a normal fault; it separates distinct regimes of tectonic and volcanic activity within the Laguna del Maule volcanic field. Faults have been imaged in lake sediments. Other north–south cutting faults are found within the Campanario Formation and the tectonic Las Loicas Trough is associated with Laguna del Maule and passes southeast of it. Some faults at Laguna del Maule may be linked to the northern termination of the Liquiñe-Ofqui Fault Zone.

Northeast of Laguna del Maule is the Cerro Campanario, a mafic stratovolcano that is 3943 m high and was active 160,000–150,000 years ago. The volcanoes Nevado de Longavi, Tatara-San Pedro and the caldera Rio Colorado lie west of Laguna del Maule; the latter two may be part of a volcano alignment with Laguna del Maule. The local volcanoes are in a segment of the crust where the Wadati–Benioff zone is 90 km deep. More distant are the Calabozos caldera and a late Pleistocene system with domes and flows south of Cerro San Francisquito, which are both silicic volcanic systems. The activity of Tatara-San Pedro and Laguna del Maule with the presence of rhyolite may be influenced by the subduction of the Mocha Fracture Zone, which projects in the direction of these volcanic centres. Nearby are the Risco Bayo and Huemul plutons, which are about 6.2million years old and may have formed through volcanism similar to that of Laguna del Maule.

Composition of erupted rocks
Laguna del Maule has erupted andesite, basaltic andesite, basalt, dacite, rhyodacite and rhyolite, the andesites and basaltic andesites define a rock suite with medium potassium contents. In the Loma de Los Espejos rocks a content of 75.6–76.7% by weight has been noted. After deglaciation, the composition of Laguna del Maule volcanic rocks has grown more silicic; since 19,000years ago, andesite eruptions have been restricted to the edges of the volcanic field. Generally, the postglacial phase of activity has generated about 6.4 km3 of rhyolite and 1.0 km3 of rhyodacite. Of the more than 350 km3 of volcanic rock in the Laguna del Maule field, about 40 km3 were emplaced postglacially. Laguna del Maule magmas contain large amounts of water and carbon dioxide; postglacial magmas on average consist of 5–6% water by weight with some variation between individual eruptions. Flushing of the magma with carbon dioxide may be important for starting eruptions.

Several stratigraphic units have been distinguished at the volcanic field, including the Valley unit exposed in the Maule valley and the Lake unit found around the lake. The Valley unit's rocks are basaltic andesite. Plagioclase and, in lesser measure, clinopyroxene and olivine form its phenocrysts. The Lake unit is mostly postglacial and includes glassy rhyolite, which is poor in crystals. Phenocrysts in the postglacial rocks are biotite, plagioclase and quartz. Mafic rocks occur as discrete rock fragments in the rhyolitic units. Microlites in the Lake unit rocks include biotite, plagioclase and spinel. Variable vesicular texture has been noted on rocks erupted during different eruptions. Temperatures of the postglacial magmas have been estimated at 820 - 950 C. The Holocene rhyolites are glassy and contain few crystals.

The postglacial rocks are composed of similar elements. High aluminium (Ai) and low titanium (Ti) are present in the basaltic andesite and basalt, a typical pattern for basic rocks in zones where plates converge. The rocks overall belong to the calc-alkaline series, although some iron-rich rocks have been attributed to the tholeiitic series. Strontium (Sr) isotope ratios have been compared to the ones of Tronador volcano; additional compositional similarity is found to other volcanoes close to Laguna del Maule such as Cerro Azul and Calabozos. Laguna del Maule stands out for the frequency of rhyolitic rocks, compared to volcanoes farther south in the chain. There are compositional trends in the region of the volcanic arc between 33° and 42°; more northerly volcanoes are more andesitic in composition while to the south basalts are more frequent.

Magma genesis
The postglacial activity appears to originate from a shallow silicic magma chamber beneath the caldera. Research published in 2017 by Anderson et al. indicates that this system is somewhat heterogeneous with distinct compositions of magmas erupted in the northwesterly and southeasterly parts of the volcanic field. The early post-glacial rhyodacites contain mafic inclusions implying that mafic lavas exist but do not reach the surface. From Sr isotope ratios it has been inferred that the magma is of deep origin, and the rare-earth element composition shows no evidence of crustal contamination. Neodymium (Nd) and Sr isotope ratios indicate all rocks are derived from the same parent source, with the rhyolites forming by fractional crystallization of the basic magma, similar to the postulated origins of rocks from the Central Volcanic Zone. Partial melting may also be the source of the rhyolites. Overall the environment where the rocks formed appears to be an oxidized 760 - 850 C hot system that formed over 100,000 to 200,000years, and was influenced by the injection of basaltic magma. The rhyolitic melts may originate in a crystal rich mush beneath the volcanic field and probably in at least two magma chambers. A minimum long-term magma supply rate of 0.0005 km3/yr has been estimated.

Obsidian
In pre-Columbian times, Laguna del Maule was an important source of obsidian for the region, on both sides of the Andes. Finds have been made from the Pacific Ocean to Mendoza, 400 km away, as well as at archaeological sites of Neuquén Province. Obsidian forms sharp edges and was used by ancient societies for the production of projectiles as well as cutting instruments. In South America, obsidian was traded over large distances. Obsidian has been found in the Arroyo El Pehuenche, Laguna Negra and Laguna del Maule localities. These sites yield obsidians with varying properties, from large blocks at Laguna del Maule to smaller pebbles probably carried by water at Arroyo El Pehuenche.

Climate and vegetation
Laguna del Maule lies at the interface between a semi-arid, temperate climate and a colder montane climate. Average yearly temperatures from 2007 to 2013 ranged from 8.1 - 10.3 C. Annual precipitation reaches about 1700 mm/year; precipitation related to cold fronts falls during autumn and winter, although occasional summer storms also contribute to rainfall. Laguna del Maule is subject to the rain shadow effect of mountains farther west, which is why the numerous summits more than 3000 m high around the lake are not glaciated. Most of the lake water comes from snowmelt; for much of the year the landscape around the lake is covered with snow.

The area of Laguna del Maule was glaciated during the last ice age. A glacial maximum occurred between 25,600 ± 1,200 and 23,300 ± 600 years ago, during which 80 km ice cap covered the volcano and the surrounding valleys. Probably due to changes in the position of the Westerlies, after c. 23,000years ago the glaciers retreated above Laguna del Maule. The glaciation has left moraines and terraces in the area, with undulating hills lying close to the outlet of the lake. Poorly developed moraines with the appearance of tiny hills lie downstream of Laguna del Maule, and form small hills around the lake rising about 10-20 m above the lake level. Other climate changes in the Holocene such as the Little Ice Age are recorded from sediments in Laguna del Maule, such as a humid period in the 15th to 19th centuries.

The landscape around Laguna del Maule is mostly desertic without trees. Vegetation around Laguna del Maule is principally formed by cushion plants and sub-shrubs; at higher altitudes vegetation is more scattered. The rocks around Laguna del Maule host a plant named Leucheria graui, which has not been found elsewhere.

Eruptive history
Laguna del Maule has been active since 1.5million years ago. Its average magma volcanic output rate has been estimated to be 200000 m3/yr—comparable to other volcanic arc systems. Eruptions occur about every 1,000 years and it has been inferred that eruptions lasted between 100 and more than 3,000days. Eruptions include both caldera-forming events and eruptions that did not leave a caldera.

Three caldera-forming events have occurred during the system's lifespan. The first took place 1.5million years ago and produced the dacitic Laguna Sin Puerto ignimbrite, which is exposed northwest of Laguna del Maule lake. The second occurred between 990,000 and 950,000years ago and produced the Bobadilla caldera and a rhyodacitic ignimbrite, also known as the Cajones de Bobadilla ignimbrite. This ignimbrite reaches a thickness of 500 m and borders Laguna del Maule lake in the north, extending about 13 km away from it. The Bobadilla caldera is centred beneath the northern shore of Laguna del Maule, and has dimensions of 12 x. The third took place 336,000years ago and produced the welded Cordon Constanza ignimbrite.

The 36 rhyodacitic lava domes and flows which surround the lake were erupted from about 24individual vents. The eruptions began 25,000years ago, after the onset of deglaciation, and continued until the last such eruption approximately 2,000years ago. After deglaciation 23,000–19,000years ago, two pulses of volcanism occurred at Laguna del Maule, the first 22,500–19,000years ago and the second in the middle-late Holocene. A first, large Plinian eruption formed the rhyolite of Laguna del Maule measuring 20 km3 from a vent presumably located below the northern part of the lake.

The Cerro Barrancas centre became active circa 14,500 ± 1,500 years before present and was the main site of volcanic activity between 14,500 and about 8,000years ago. After that point activity shifted and the volume output increased; the subsequent units have a volume of 4.8 km3. These two phases of volcanic activity occurred within 9,000years of each other and the magmas involved may have been sourced from different magma reservoirs.

Undated postglacial units are andesitic Crater Negro scoria cone and lava flow just west of Laguna del Maule, andesitic Playa Oriental on the southeastern shore of Laguna del Maule, rhyolitic Arroyo de Sepulveda at Laguna del Maule and rhyodacitic Colada Dendriforme (unit rcd ) in the western part of the field. This rhyolitic flare-up is unprecedented the history of the volcanic field, and it is the largest such event in the southern Andes. It took place in two stages, a first early after deglaciation and a second during the Holocene, which featured magmas with distinct composition.

Three mafic volcanic vents named Arroyo Cabeceras de Troncoso, Crater 2657 and Hoyo Colorado are also considered postglacial. The former two are andesitic, while the latter is a pyroclastic cone. Mafic volcanism appears to have decreased after glacial times at Laguna del Maule, probably because such magmas were hindered from ascending by a more silicic magma system, and the post-glacial volcanism has a mainly silicic composition. The magma chamber acts as a trap for mafic magma, preventing it from rising to the surface and thus explaining the absence of postglacial mafic volcanism.

Explosive eruptions and far-field effects
Explosive activity including ash and pumice has accompanied a number of the postglacial eruptions; the largest is associated with Los Espejos and has been dated to 23,000years ago. The deposit of this Plinian eruption reaches 4 m of thickness at a distance of 40 km. White ash and pumice form layered deposits east of the Loma de Los Espejos; another explosive eruption is linked to the Barrancas centre. Other such explosive events have been dated at 7,000, 4,000 and 3,200years ago by radiocarbon dating. About three Plinian eruptions and three smaller explosive eruptions have been identified at Laguna del Maule; most of them took place between 7,000 and 3,000years ago. It has been estimated that the ash and pumice deposits have a volume comparable with that of the lava flows.

A tephra layer in the Argentine Caverna de las Brujas cave dated 7,780 ± 600 years ago has been tentatively linked to Laguna del Maule, and another with a thickness of 80 cm that is 65 km away from Laguna del Maule is dated 765 ± 200 years ago and appears to coincide with a time with no archaeological findings in the high cordillera. Other tephras that possibly were erupted at Laguna del Maule have been found in Argentinian archaeological sites, one 7,195 ± 200 years ago at El Manzano and another 2,580 ± 250 to 3,060 ± 300 years old at Cañada de Cachi. The El Manzano tephra reaches a thickness of 3 m about 60 km away from Laguna del Maule and would have had a severe impact on Holocene human communities south of Mendoza.

Most recent activity and geothermal system
The most recent dates for eruptions are ages of 2,500 ± 700, 1,400 ± 600 and 800 ± 600 years for rhyolitic lava flows, with the last eruption forming the Las Nieblas flow. No eruptions have occurred during historical time, but petroglyphs in Valle Hermoso may depict volcanic activity at Laguna del Maule.

Laguna del Maule is geothermally active, featuring bubbling pools, fumaroles and hot springs. Temperatures in these systems range between 93 - 120 C. There is no degassing at the surface but emission of gas bubbles has been observed in Laguna del Maule lake. The Baños Campanario hydrothermal springs lie northwest from Laguna del Maule and their waters together with these from the Termas del Medano springs appear to form through a mixing of magmatic and precipitation water. The field has been evaluated as a potential source of geothermal energy. It and the neighbouring Tatara-San Pedro volcano form the so-called Mariposa geothermal system discovered in 2009, whose temperature has been estimated on the basis of gas chemistry to be 200 - 290 C and which features fumaroles. One estimate puts the potential productivity of Laguna del Maule as an energy source at 50 - 200 MW.

Possible future eruptions
The Laguna del Maule volcanic system is undergoing strong deformation; uplift between 2004 and 2007 attracted the attention of the global scientific community after it was detected by radar interferometry. Between January 2006 and January 2007 uplift of 18 cm/yr was measured, and uplift during 2012 was about 28 cm. Between 2007 and 2011 the uplift reached close to 1 m. A change in the deformation pattern occurred in 2013 related to an earthquake swarm that January, with deformation slowing through to mid-2014 at least. Measurements in 2016 indicated that the uplift rate was 25 cm/yr; uplift has continued into 2019 and the total deformation has reached 1.8 m to 2.5 m. This uplift is one of the largest in all volcanoes that are not actively erupting; the strongest uplift worldwide was recorded between 1982 and 1984 at Campi Flegrei in Italy with an end change of 1.8 m. Other actively deforming dormant volcanoes in the world are Lazufre in Chile, Santorini in Greece from 2011 to 2012, and Yellowstone Caldera in the United States at a rate of 1/7th that of Laguna del Maule. Another South American volcano, Uturunku in Bolivia has been inflating at a pace 1/10th that of Laguna del Maule's. There is evidence that earlier deformations occurred at Laguna del Maule, with the lake shores having risen by about 67 m during the Holocene possibly as a consequence of about 20 km3 entering the magmatic system.

The present-day uplift is centred beneath the western segment of the ring of post-glacial lava domes, more specifically beneath the southwest sector of the lake. The source of the deformation has been traced to an inflation of a sill beneath the volcanic field that is 5.2 km deep with dimensions of 9.0 x. This sill has been inflating at an average pace of 31000000 ± between 2007 and 2010. The rate of volume change increased between 2011 and 2012. , 2000000 m3/yr of magma are estimated to enter the magma chamber. The average recharge rate required to explain the inflation is about 0.05 km3/year. This volume change is approximately 10 to 100 times as large as the field's long-term magma supply rate. Gravimetric analysis has indicated that between April 2013 and January 2014, approximately 0.044 km3 of magma intruded beneath the field. The presence of a sill is also supported by magnetotelluric measurements indicating conductivity anomalies at depths of 4 - 5 km beneath the western side of the volcanic field and at 8 - 9 km depth beneath its northern part. They show the existence of rhyolitic melt, but they do not show a magmatic system associated with the southeastern vents, leaving their magma supply route uncertain. The existence of a Bouguer gravity anomaly also indicates the presence of a low-density body 2 - 5 km beneath the volcano. Seismic tomography has found a 450 km3 magma reservoir centered beneath the northwestern part of the lake, at 2 - 8 km depth. It may contain about 5% melt and has a heterogeneous structure with varying melt fractions in various parts of the reservoir. A reservoir of crystal-rich mush estimated as having a volume of 115 cubic kilometres (28 cu mi), with about 30 cubic kilometres (7.2 cu mi) of magma embedded within the mush, may have moved away from the old vents towards its present-day position. It is being resupplied by deeper, more crystal-poor magmas. In the deep crust, further magma systems may connect Laguna del Maule with Tatara-San Pedro volcano.

Seismicity
Strong seismic activity has accompanied the deformation at Laguna del Maule. Seismic swarms have been recorded above the depth of the deforming sill south of the ring of lava domes, particularly around Colada Las Nieblas. A magnitude 5.5 earthquake occurred south of the volcanic field in June 2012. A major volcano-tectonic earthquake swarm occurred in January 2013, possibly due to faults and underground liquids being pressurized by the intrusion of magma. Between 2011 and 2014, swarms of earthquakes occurred every two or three months and lasted from half an hour to three hours. Most earthquake activity appears to be of volcano-tectonic origin, while fluid flow is less important; two intersecting lineaments on the southwest corner of the lake appear to be involved. The 2010 Maule earthquake, 230 km west of Laguna del Maule, did not affect the volcanic field; the rate of uplift remaining unchanged, while other measurements indicate a change in the uplift rates at that point. Although some shallow earthquakes have been interpreted as reflecting diking and faulting on the magma chamber, the pressure within the chamber appears to be insufficient to trigger a rupture all the way between the surface and the chamber and thus no eruption has occurred yet.

Potential mechanisms for the uplift
Several mechanisms have been proposed for the inflation, including the movement of magma underground, the injection of new magma, or the action of volcanic gases and volatiles which are released by the magma. Another proposal is that the inflation may be situated in a hydrothermal system; unless the Baños Campanario 15 km away are part of a hydrothermal system, there is little evidence that such a system exists at Laguna del Maule. Carbon dioxide anomalies, concentrated on the northern lakeshore, have been found around Laguna del Maule, possibly triggered by the stress of the inflation activating old faults. These anamolies may indicate that the inflation is of mafic composition, as rhyolite only poorly dissolves. Gravity change measurements also show an interaction between magma source, faults and the hydrothermal system.

Hazards and management
This uplift has been a cause of concern in light of the history of explosive activity of the volcanic field, with 50eruptions in the last 20,000 years; the current uplift may be the prelude of a large rhyolitic eruption. In particular, the scarce fumarolic activity implies that a large amount of gas is trapped within the magma reservoir, increasing the hazard of an explosive eruption. It is not clear if such an eruption would fit the pattern set by Holocene eruptions or would be a larger event. The prospect of renewed volcanic activity at Laguna del Maule has caused concern among the authorities and inhabitants of the region. A major eruption would have a serious impact on Argentina and Chile, including the formation of lava domes, lava flows, pyroclastic flows near the lake, ash fall at larger distances and lahars. The international road across Paso Pehuenche and air traffic in the region could be endangered by renewed eruptions. Laguna del Maule is considered to be one of the most dangerous volcanoes of the Southern Andean volcanic belt. In March 2013, the Southern Andean Volcano Observatory declared a "yellow alert" for the volcano in light of the deformation and earthquake activity; the alert was supplemented afterwards with an "early" warning (withdrawn in January 2017). The Chilean National Geology and Mining Service monitors the volcano and a preliminary hazard map has been published.