Geophysical Footprints of Cotopaxi’s Unrest and Minor Eruptions in 2015: An Opportunity to Test Scientific and Community Preparedness
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Cotopaxi volcano, Ecuador, experienced notable restlessness in 2015 that was a major deviation from its normal background activity. Starting in April and continuing through November 2015 strong seismic activity, infrasound registry, hikes in SO2 degassing and flank deformation with small displacements were some of the geophysical anomalies that were registered. Obvious superficial changes, such as small hydromagmatic eruptions, emission of vapor and ash columns, thermal hotspots around the crater and in nearby orifices and exacerbated glacier melting were also observed. Our contribution provides an overview of the 2015 Cotopaxi unrest by presenting the patterns of geophysical data and the sequence of events produced by the volcano. Cotopaxi’s last important VEI 4 eruption was in 1877. Then it had devastating effects because of the transit of huge lahars down 3 major drainages. Comparatively, the 2015 activity never surpassed a magnitude VEI 2 and principally produced limited hydromagmatic explosions and semi-continuous low energy emissions and light ashfalls. Given the potential of major destruction from a large Cotopaxi eruption it is important to understand the geophysical fingerprints that characterized the 2015 episode with an eye to identifying onset of future restless periods. Overall, the monitoring activities, the data interpretation, formulation of reasonable eruptive scenarios, and finally, the preparation of a stream of constant information being relayed to concerned authorities and the public, was a real test of the IGEPN’s capacity to deal with a complicated eruption situation whose outcome was not apparent at the beginning, but which concluded in a very small eruptive episode.
KeywordsVolcanic unrest Precursory geophysical patterns Precursory LPs and VLPs Volcano monitoring Cotopaxi volcano-Ecuador State of preparedness
En 2015 el volcán Cotopaxi, Ecuador experimento un notable cambio, que fue una desviación importante de su actividad normal de base. A partir de abril y hasta noviembre de 2015 fuerte actividad sísmica, registros de infrasonido, incremento en la desgasificación de SO2 y pequeños cambios en la deformación de los flancos fueron algunas de las anomalías geofísicas registradas. Evidentes cambios superficiales también fueron observados como pequeñas erupciones hidromagmaticas, emisión de vapor, columnas de cenizas, puntos calientes alrededor del cráter y el deshielo de los glaciares. Nuestra contribución proporciona una visión general de las anomalías del Cotopaxi en el 2015, mediante la presentación de patrones de los datos geofísicos y la secuencia de eventos producidos por el volcán. La última erupción importante del Cotopaxi fue un VEI 4 en 1877. Esta tuvo efectos devastadores debido al descenso de enormes lahares por sus tres drenajes mayores. Comparativamente, la actividad del año 2015 nunca superó una magnitud VEI 2, principalmente produciendo explosiones hidromagmaticas, escasas emisiones y leves caídas de ceniza. Debido a la potencial destrucción por una eventual erupción grande del Cotopaxi es importante entender los registros geofísicos que caracterizó el episodio de 2015 para poder identificar el inicio de futuros períodos eruptivos. En general, las actividades de vigilancia, la interpretación de datos, formulación de escenarios eruptivos razonables y por último, la preparación de un flujo de información constante que llegue a las autoridades interesadas y el público, fue una verdadera prueba de la capacidad del IGEPN para hacer frente a una situación de erupción cuyo resultado no era evidente al principio, pero que finalizó como una erupción pequeña.
Long dormant volcanoes that begin to awaken may have start and stop activity that has to be evaluated with respect to the volcano’s known past. A volcano’s past activity is known by study of its stratigraphy, other physical evidence and possibly historical chronicles (Tilling 1989). Many uncertainties preclude knowing the final outcome of a restless volcano (Newhall 2000; Sparks and Aspinall 2004), since a volcano may awaken for short term low-level activity, then resume repose until additional magma inputs herald an episode of further unrest (Phillipson et al. 2013). Eruptions that barely bring magma to the surface may be classified as “failed”, since so little juvenile magma erupts (Moran et al. 2011).
At Cotopaxi ample geological and historical information exists with regard to its past activity (Hall and Mothes 2008; Garrison et al. 2011; Pistolesi et al. 2012). Formulation of eruptive scenarios with respect to the 2015 unrest period were based on our collective knowledge of the volcano’s geology and eruptive history and published information as well as interpretation of the abundant geophysical data streams available through instrumental and observational networks operated by the Instituto Geofísico of the Escuela Politécnica Nacional (IGEPN)-Quito, Ecuador, the entity in charge of volcano and tectonic monitoring in Ecuador. The combination of these inputs allowed scientists at the IGEPN to transmit a coherent image of the evolving unrest presented during 2015 and to indicate the most likely eruption/activity scenarios. Two earlier unrest periods are known: 1975–1976, when the IGEPN had limited seismic equipment operating on the volcano and then in 2001–2002. Both periods were comprised of increased fumarolic activity both inside and outside of the crater and a hike in seismicity for the 2001 period (Molina et al. 2008). The 2015 unrest displayed important changes in seismic and deformation patterns, gas output and superficial activity, compared to background, whose level was established since around 1990. In sum, Cotopaxi’s 2015 unrest displayed a progressive crescendo of geophysical signals, then minor hydromagmatic explosions, followed by overall seismic energy decrease at the end of 2015, which was accompanied by fewer superficial manifestations. Like many other volcanoes that have displayed unrest, this recent episode did not culminate in a full-fledged eruption with large volumes of juvenile pyroclastics (Phillipson et al. 2013). Moran et al. (2011) maintain that an eruption is “failed” when magma reaches but does not pass the “shallow intrusion” stage, i.e., the magma gets close to, but does not reach the surface. In the actual case, the amount of erupted material was minor, and had a dense rock equivalent volume of ~0.5 Mm3 (Bernard et al. 2016).
The volcano’s five most important eruptive episodes during the historical period (since 1532) have been of andesitic composition and ranged between VEI = 3 and 4 (Pistolesi et al. 2012). Nonetheless, the volcano is bi-modal and produces VEI = 5 rhyolitic eruptions about every 2000 years (Hall and Mothes 2008). The last important rhyolitic eruption, the Peñas Blancas event, occurred about 2800 years BP (Mothes et al. 2015a). The youngest andesitic eruptive products contain intergrowths of plagioclase and pyroxene and four different populations of plagioclase crystals which indicate pervasive magma mixing (Garrison et al. 2011).
Given the high probability for the generation of long-distance lahars, wide dispersal of pyroclastic fall, and the consequential negative impact on many economic activities and the compromise of critical infrastructure should an eruptive period last for months to years, Cotopaxi is considered a “National” volcano, located in the center of Ecuador, near to Quito, the capital and other populated areas. Even a short-lived VEI 4 eruption (VEI = Volcano Explosivity Index) (Newhall and Self 1982) has the potential to gravely affect Ecuador’s overall productivity and major transport lines. Lastly, the volcano is considered one of the most dangerous in Ecuador, given the possible exposure of >300,000 residents to primary lahars and ashfalls during future VEI = 3 or greater magnitude eruptions (Mothes et al. 2016a).
Cotopaxi has long been a producer of swarms of LP’s, and Ruiz et al. (1998) hypothesized that they were related to the interaction of the hydrothermal system with heat ascending from depth. During unrest in 2001–2002 thousands of long period, volcano-tectonic and distal volcano-tectonic seismic events were registered and magma was hypothesized to have ascended to shallow levels in the center of the edifice (Molina et al. 2008). Its flanks also experienced deformation from magma input estimated at ~20 Mm3 from modeling of EDM data (Hickey et al. 2015). But, observable superficial manifestations were meager, no magma erupted and the volcano returned to a relatively quiet state with only short-lived LP swarms (Lyons et al. 2012) and sporadic VLP events being registered until April, 2015 (Márquez 2012; Arias et al. 2015).
Cotopaxi was a VUELCO target volcano from 2013 to 2015. As part of the VUELCO project, in November 2014 a simulation exercise was carried out with the purpose of presenting a timeline of potential unrest and expected events and to test the communication between scientists, decision-makers and the public (www.vuelco.net). This present contribution is written in the spirit of holistically documenting this recent and most serious unrest of Cotopaxi to date—since 1942, when slight ash emissions and mild explosive activity were then reported (Siebert et al. 2010). Here we present the macro patterns of seismic, gas, deformation and visual observation monitoring data associated with the awakening volcano. The data are provided by the monitoring networks operated by the IGEPN. We avoid dwelling on details, as forthcoming contributions dedicated to exploiting specific datasets are in preparation. We also provide comment on selected actions in which IGEPN scientists participated to make the overall societal outcome more favorable in case Cotopaxi produced a major eruption. We impart with the philosophy, stated in Marzocchi et al. (2012) that “sound scientific management of volcanic crises is the primary tool to reduce significantly volcanic risk in the short-term”. We also maintain that a constant and rapid analysis of the monitoring data is key to giving forecasts that include reasonable scenarios. Some of the IGEPN actions were guided by experiences gained in the VUELCO project, since one of the scenarios in the simulated eruptions was that the volcano would wake up, be active then return to repose.
The 14th of August, 2015 explosions and subsequent emissions pushed the first evidence of new magma to the surface, although in a limited way (Gaunt et al. 2016). Documentation of the geophysical signals and observations that we registered through late 2015 leads to the depiction of what transpired—mainly of an intrusion, which stayed deep, although the signs of intrusions that stall at depth may be very similar to those produced by intrusions that finally do erupt (e.g. Moran et al. 2011).
Synthesis of the Geophysical Fingerprints of the Unrest
Geophysical Registry of Cotopaxi’s Restlessness in 2015
Most VLP events had frequencies between 0.1 and 1 Hz and had strong P and S waves, such as the example given for 04 August, 2015 which was located 3 km below summit on the NE flank of the volcano (Fig. 6).
Due to the westward movement on the GPS station PSTO, which is 22 km W of the crater (Fig. 10), we surmised that the source was deep. Subsequent modeling of the data suggested a source of about 24 km deep located under the SE flank with a volume of 42 ± 26 Mm3 (Mothes et al. 2016b). Nonetheless, as mentioned in Sect. 3.1, analysis of the erupted ash suggests that the magma source is shallow, as least for the initial small volume that was emitted.
Data from a tiltmeter (VC1G on Fig. 2) installed in a thick lava package and located 6 km NE of the crater, showed a strong inflationary pattern that had started in April, 2015 on both axis. This tilt anomaly coincided with the notable increase in seismicity (Mothes et al. 2016b). Generally, when LP seismicity and tremor were both strong, a positive tilt signal predominated.
Hydromagmatic Explosions/Strong Emissions of 14 August, 2015
Two months earlier public and authorities had been forewarned in the special IGEPN reports (No. 3 and 4) that phreatic explosions would be a likely phenomenon in precursory eruptive activity (http://www.igepn.edu.ec/cotopaxi/informes-cotopaxi/coto-especiales/coto-e-2015/12990-informe-especial-cotopaxi-11-06-2015/file).
Post 14 August, 2015: Open Conduit Degassing and Ash Emissions
In early September ash columns still rose to over three kilometers height above the vent and carried fine ash particles to cities on the piedmont of the coastal plain, such as Santo Domingo de los Colorados, located 120 km W of the volcano, essentially situated under the red swath trending W in Fig. 15.
Ashfall was still prevalent in mid-October, but had all but terminated the third week of November where it was seen W-NW of the volcano. VAAC Washington again reported suspended fine ash above Santo Domingo as well as in Los Rios province to the SW. The ash column generally rose to only 1 and 3 km above the summit and had a velocity between 6 and 10 m/s and lasted about one week. Fieldwork permitted the estimation of a mass and volume total of 3.49 × 107 kg (22,100 m3) for this late, waning period (Bernard et al. 2016). The total ashfall dense rock equivalent (DRE) volume for the entire eruption was calculated in 0.5 Mm3 (Bernard et al. 2016).
Analysis of ash beneath both binocular and scanning electron microscope showed clearly that there was an evolution in ash componentry from the eruption’s beginning on 14 August and later. The first ash from 14 August had more hydrothermal lithics (pyrite, scoria with vesicles filled with altered material and hydrothermal quartz). As the eruptions progressed we saw an increase in more fresh magmatic components, such as free crystals, glass particles with low vesicularity and a high percentage of microlites, which implied low magma ascent rates and stiffening of magma in the upper part of the column (Gaunt et al. 2016).
Ashes collected on the 20th of October, had a high concentration of dense microcrystalline material. Although there is evidence of few vesiculated clasts (diktytaxitic texture); about 65% of the ash is considered possibly juvenile. Gaunt et al. (2016) suggest that the origin of the ash is the top of a degassed magma column which had ascended from about 3 km below the crater.
For most of the post explosive period after mid-August, seismic hypocenters still remained located at the two depths mentioned above (Fig. 7). Most relevant was the sporadic occurrence of VT events with magnitudes of 3 or greater that occurred. Sometimes spasmodic tremor was registered and continued for hours, as for example, that registered on 02 September, 2015.
Visual Observations and Secondary Effects
On September 3, water emerging from the basal fronts on the northern glaciers was clearly observed, and countless new crevices in the majority of glacier ends and on the upper flanks were evident. All this led to the conclusion that an abnormal process was producing increased melting of the glaciers. Starting in mid September it was possible to observe the presence of small secondary lahars descending several streams and we estimated that many of them were due to increased glacier melting.
Orthophotos made on August 18 and then again on October 8, show a decrease of about 0.49 km2 of the area covered by glaciers. This represents a very high rate of glacier melting, not explained exclusively by climate change (Cáceres et al. 2016).
We estimate that small volumes of magma reached surface levels in the volcano conduits causing increased circulation of hot fluids inside the edifice, apparently reaching the basal area of the glaciers and producing increased melting. It is necessary to further investigate the hazard due to instability in the melting glaciers and their eventual collapse that could lead to greater secondary lahars. Numerical modeling by Hemmings et al. (2016) has shown the importance of hyrdrothermal perturbations at Cotopaxi in generating watery flows.
Incandescence was also occasionally observed on cold still nights with a thermal camera or by simple vision. These events were considered to have been caused by pulses of hot gases.
The glacier around the crater, on the W and N flanks, became partially covered by ash. This coating of dark ash decreased the glacier albedo and consequently increased the absorption of solar rays. Therefore expedite melting of the glacier tongues increased, leaving obvious melt water channels issuing from the glaciers’ base.
As a result of the afternoon melting by insolation and perhaps also by higher temperatures of the rock beneath the glaciers, runoff increased, especially off the W flank glaciers and there were frequent small secondary lahars. Those lahars that have been especially associated with rain storms obtained the highest discharges—on the order of 10–30 m3/sec (D. Andrade-IGEPN, Pers, Comm, 2015). The Agualongo channel, on Cotopaxi’s W side was frequently flooded by lahars and on three occasions they covered partially the main road giving access to the volcano.
Interpretation and Model
As shown in Fig. 16, LP events gradually increased starting in April, 2015, beginning with small magnitudes and low energy levels (Fig. 3). We interpret the LPs to imply fluid movement occurring at 10–12 km below the crater and then up to shallower levels (Fig. 7). There were only scarce VTs that occurred in concert with the LPs. In late May VLPs were registered (Fig. 5) and were interpreted to be possible mass magma transport processes as reported by Arias et al. (2015). Often VLPs are identified as eruption precursors, e.g. at Redoubt (Power et al. 2012), for example. In hindsight, vigorous VLPs were also registered in 2009–2010 at Cotopaxi and correlated with recoverable deformation patterns at borehole tilt stations (Mothes et al. 2010), but did not result in an extended seismic crisis or magmatic activity on the surface.
Nonetheless, LP and VLP events registered in April–August, 2015 were apparently responding to a slow ascent of a small magma slug and associated fluids and in April 2015 deformation recorded by tilt and GPS stations began almost synchronically with the jump in LP seismicity, implying that there may already have been magma ascent from a deeper depth to a shallower reservoir in order to show changes on the most proximal tiltmeters. The GPS stations begin to show minor displacements at the same time, particularly on the W-SW flank, where no strong evidence was detected in seismicity, but to the contrary seismicity was concentrated more on the E-SE flanks (Fig. 7). In sum, we registered both shallow and deep seismic activity. A leading hypothesis for this pattern likely was the interaction between fluids being released by a deep-seated source, say at 24 km depth as proposed in our geodetic model. These fluids ascended and perturbed a preexisting shallow-seated source, which may be the magmatic remnant that drove the 2001–2002 unrest reported by Hickey et al. (2015).
With more new magma in Cotopaxi’s system, SO2 output became prevalent in mid-May, one month after the hike in seismicity. Background SO2 levels of <500 ton/day were surpassed and rose to over 3000 ton/day. The strong onset of bands of tremor about the 1st of June, were conjectured to be related to continual fluid movement within the edifice and perhaps to the boiling of the hydrothermal system and was a signal that more overall heat was circulating within the edifice.
Along with the rise in SO2 there was also a trend in production of more VLP’s since 114 of these events were registered between May and mid-August, 2015. Of great significance is that the largest VLPs were registered in the last 3 weeks before the hydromagmatic explosions. Afterwards too there were infrequent VLP’s (Fig. 5).
With the highest energy levels of the VLPs being logged before the explosions, these events seem to have been one of the detonators of the explosions (Fig. 5b). They seemed to herald that magma/fluids were ascending. Of particular note was the VT/LP swarm of the 13th–14th of August that began 12 h before the hydromagmatic eruptions on the morning of 14 August (Fig. 11). The swarm comprised of some 40 VTs and >50 LPs was the most energetic of any seismic swarm registered at Cotopaxi since 2002 and was a warning in hindsight which presaged the subsequent explosions/strong emissions some hours later. These seismic trends and the higher SO2 flux, would indicate that magma was working in the upper part of the system—at least in the 0 to 6 km level below the crater.
The initial explosions had a phreatic component since water was available in the small pond at the crater’s base, sub-glacial melting and from pore water within the hydrothermal system. Nonetheless, Gaunt et al. (2016) argued that the most likely driving force of the initial explosions was magmatic heat interacting with the hydrothermal system providing energy to trigger hydromagmatic eruptions at Cotopaxi. Textural evidence for this process was only preserved in the deposits of the initial eruptions, but not subsequent ones. Later emissions were likely the result of the repeated formation and destruction of a shallow magmatic plug by brittle fragmentation through mechanical stresses and decompression. Gas overpressure must have been accumulating beneath the conduit plug and may have contributed to the flank deformation, particularly as registered by the tiltmeters. In the succeeding post-explosion days SO2 output rose to 16,000–18,000 ton/day (Hidalgo et al. 2016), a likely testimony to the accumulated gas that had been trapped in the plumbing system.
The expulsed material showed evidence of strong hydrothermal alteration and there was initially little evidence of juvenile components. There was also a low pH (3.6–5.1) and high sulfate- SO4 concentrations (up to 13,000 mg/kg) in the expulsed ashes of the 14th to 25th of August, as detected by leachate analysis (P. Delmelle, Pers. Comm, 2015). Later, as described above, the percentage of juvenile components increased through time, to the last erupted material collected in late November, 2015.
After the explosions and strong emissions of the 14th of August, the conduit lost its retaining plug and remained open and continual fluid movement was facilitated, although pulsatile superficial activity continued, and few shallow explosions occurred. After the explosions LP events were initially high (>200 events/day), but dropped to <20 events/day by the first week of September, where they remain at this writing.
While the LPs diminished, to the contrary the VT events rose notably. Around the 1st of September 15–20 LP events/day were registered. By the third week of September these increased to >200 events/day (Fig. 16), and subsequently this value decreased to 50–100 events/day, but in all totaled nearly 15,000 events. In the last 3 months of 2015 persistent VT daily activity was registered as well as waning tilt and GPS offsets. Even with the VT swarm overall seismic energy levels decreased compared to the levels registered in May to August, which may be due to the overall successful degassing of the system, but could also be explained by closing of the conduit by a degassed magma column, thus impeding freer liberation of gases. Between October 2015 through April, 2016 internal explosions of deep providence were registered at a rate of 20–30 such events/month. These explosions could be interpreted as gas passing through restrictive areas within the conduit. While displaying only minimal infrasound and no detectable superficial vestiges, these explosions may be occurring due to pressurization deep within the system (e.g. Valentine et al. 2014).
The Science-Society Interface
Strong evidence points to a magmatic component in Cotopaxi’s 2015 reactivation and that this may be a precursor for future episodes, given that the bulk of the new magma that perturbed the system remained at depth. As a comparison, the 2001–2002 restless period had essentially been internal with only the weakest of superficial manifestations. For the 2015 reactivation IG scientists took the warnings very seriously and put all their collective experience to the test to make interpretations of the monitoring data and to manage successfully the great expectations of the public and authorities during the crisis period described above. Overall IGEPN volcanologists wrote 23 special reports that were disseminated via multiple media (www.igepn.edu.ec). Given the low levels of acceleration of seismic energy, small ground displacements and visual observations, eruption scenarios that the IGEPN formulated stayed within the realm of VEI 1–2 levels and clearly stated that the least likely scenarios was the generation of a paroxysmal eruption in which PDC’s, voluminous ashfalls and giant lahars would be formed.
With each convincing sign that Cotopaxi was displaying stronger activity, IG scientists were proactive in improving and strengthening all monitoring systems while simultaneously helping to prepare the populations and authorities for what a major eruption of Cotopaxi could mean. Work by Christie et al. (2015) (an earlier VUELCO contribution) had shown that residents of the Chillos valley, to the east of Quito, were particularly ill-prepared to confront lahar hazards due to their recency of living in that valley. On the other hand, residents of the Latacunga valley had a clearer memory of lahar hazards, since many of their distant relatives had lived through Cotopaxi eruptions and their collective memory is better preserved. Nonetheless, social media, both beneficial and alarming, steered perceptions and actions of residents. The area of influence by the volcano, especially with respect with lahars, includes four important provinces, several counties and Quito’s jurisdiction. It was particularly difficult to meet the demands and expectations and provide the personal attention of monitoring scientists to the authorities in each of these different municipalities as well as to meet with other community groups and respond to their uncertainties. There were also the constant attacks on social media of several particularly meanly-intentioned individuals who constantly tried to steer attention away from the IGEPNs scientific work by saying that it was operating with poor instrumentation or that the monitoring work at IGEPN was “carried out by amateurs”.
All told, IGEPN scientists provided abundant custom guidance to local and national officials and residents with regards to volcano hazards and the proposed scenarios. A total of about 125 talks were given by IGEPN personal during the unrest period. Additionally, there was broad coordination with Ecuador’s Secretary for Risk Management at all levels and participation in guiding eruption simulations. Some of the discussions with them were based on what had been reviewed in the VUELCO workshop-simulated eruption exercises carried out in late 2014 in Quito. The IGEPN also greatly benefitted by the strong collaboration and presence of members of the USGS/USAID Volcano Disaster Assistance Team who led informed discussions on the trends of the geophysical precursors and also helped to reinforce the lahar-detection network. Personal from Chalmers University of Technology (Sweden), JICA (Japan), IRD (France) and NASA (USA), DEMEX-EPN with help in SEM, LMU-Germany with grain size x-ray diffraction and UCL (Belgium) with leachates, also collaborated during the crisis.
As the eruption process waned, it was obvious that high-risk populations were tired of being constantly alert and didn’t want to be perpetually attentive to volcanic processes that could threaten their livelihoods and families. This issue will have to be acknowledged and dealt with in future reactivations.
Seismic activity and its evolution in event types, energy release, shallowing depths and locations, elevated degassing and ash emissions and flank deformation typified the restlessness of Cotopaxi during 2015. The important accumulative energy release first of LPs than followed by registry of an important suite of large VLP’s was a significant geophysical pattern indicating fluid movement, followed then by a more convincing transfer up conduit of small slugs of magma and gases to beneath the conduit plug. In the late hours of the 13th of August this plug fractured and ruptured, evidenced by the vigorous swarm of VTs and LPs before the hydromagmatic explosions that occurred early on the 14th of August 2015. Minor ground deformation, the small, limited explosions in August and subsequent ash emission suggest that the ascended magma volume was small, and indeed as calculated by Bernard et al. (2016), was only about 0.5 Mm3 DRE. This value is far inferior to the possible volume of 42 ± 26 Mm3, which is hypothesized to be at depth based on modeling of the observed GPS displacements (Mothes et al. 2016b). A second energetic magmatic pulse did not arise, and certainly not one with a sufficient volume to produce a VEI 3 or 4 eruption, which was one of the least likely scenarios, but nonetheless dreaded by the society and scientists.
Following the 14 August explosions and subsequent ash emissions we did not observe a new phase of outward GPS displacement trends in the deformation data, which could have implied a new magma input to cause another phase of deformation. The post-explosion VT seismic swarm which lasted 5 months was indicative of persistent internal perturbation but did not transpire in a new phase of deformation, thus we assumed that we were dealing with a small magma volume. The magma that tipped off the 2015 unrest may have been a remnant of that which provoked the 2001–2002 episode and was reported by Hickey et al. (2015). This residual magma could have been disturbed by the ascending heat and fluids from the new magma input at depth (~24 km) whose source was possibly under the SE flank, and which provoked the recorded ground deformation and the LP and VLP seismicity.
The volcano was benevolent and had awakened to only a VEI 2 level. No major damage was imparted upon the population or on livelihoods, except for temporary local economic depression, increased anxiety of the population, mild crop losses and premature selling of livestock due to fears of future losses. Overall, the volcano’s manifestations served as a warning to everyone to keep attentive of Cotopaxi’s capacity to cause destruction and possible severe ruin by lahar transit down major drainages which are heavily populated and host important strategic infrastructure.
An eruption process can last months to decades, and we need only to look at Tungurahua, an andesitic stratocone also in Ecuador’s Cordillera Real, with ongoing eruptions for 17 years (Mothes et al. 2015a, b), or Soufrière Hills on Montserrat (Sparks and Young 2002) to suggest that the next round of Cotopaxi eruptions could last more than just several months. In the case of Tungurahua, activity started gradually in 1999 and displayed oscillating low-level behavior over the years to finally generate a rapid-onset VEI 3 eruption in 2006 (Hall et al. 2013). Such long waits test the population’s resilience, but is also a time for monitoring scientists to become acquainted with the volcano’s eruption style. During a reactivation period of a long dormant volcano there are many uncertainties and this demands stringent work and continual mindfulness by monitoring scientists and frequent ongoing interactive and personal communication with local communities and authorities.
During the 2015 unrest period at Cotopaxi, people living in high-risk zones (i.e. Latacunga and Valle de los Chillos) were swayed by speculation, rumors and lies concerning the status of the volcano. Some people also tended to weigh-in toward imprecise information posted on Facebook or Twitter and heed pseudo volcanologists and detractors, rather than rely on information from official channels. It was not uncommon to receive telephone calls from hysterical residents in either of these population centers inquiring if a Cotopaxi eruption was imminent? All told the IGEPN put out 3 reports each day about the volcano’s activity and more than 24 special reports, all which are available on the IG website (www.igepn.edu.ec). The number of followers on the IGEPN’s Facebook page grew to >1 million. To help stem the flow of bad information at the community level Ecuador’s 911 system, in coordination with IGEPN personal, formed a pan-volcano vigía network comprised of volunteer observers who report via radio several times a day about their visual and audible observations of Cotopaxi or the rivers that are borne on it. This network with 55 volunteers, is in many ways a replica of the successful community-based vigía system that has functioned at Tungurahua volcano since 2001 (Stone et al. 2014; Mothes et al. 2015b). The information provided by the vigía volunteers compliments the ongoing geophysical monitoring and also serves to strengthen their capacities as community leaders and guides during volcano crisis (Espín Bedón et al. 2016).
A hypothesis for a future trend in activity weighs heavily towards hydromagmatic to Vulcanian explosions which may have a rapid onset, similar to the 14th of August episode, then evolve to sub-Plinian to Plinian eruptions of VEI 3–4 magnitude, if enough magma has accumulated at a relatively shallow depth (maybe 0–7 km below the crater) as shown in Fig. 7 for the upper level seismicity, and can make it to the surface before degassing. Vulcanian eruptions have been prominent in the volcano’s historical activity (Gaunt et al. 2015). Unraveling the story will be difficult.
As the volcano is well-monitored 24 h/day/365, we anticipate that the IGEPN will provide early warnings to the public and officials before onset of important eruptive activity. This 2015 “dry run” allowed for diversification and hardening of Cotopaxi’s monitoring network, frequent preparation and reappraisal of eruption scenarios and for the creation of a society-wide discussion of the possible consequences of a large Cotopaxi eruption. Some of these steps were facilitated by previous work in a VUELCO workshop. Essentially, attending to the 2015 activity was an opportunity to test the level of preparedness of the scientists and of the Ecuadorian society. All IGEPN scientists strived hard to be ready to “call it right”, had the occasion arisen and a large eruption was in preparation. Since so little new magma erupted and there was no detectable subsequent shallow magmatic recharge, we consider the eruption as extremely small, and that the residual magma is in repose until a future time. Overall, the crisis was an important opportunity for learning about Cotopaxi’s restlessness, with particular recognition of the increase in the VLP events and their energy levels just weeks before the mid-August explosions and the synchronous but progressive ground deformation signals, albeit small, that coincided with the increased seismicity. These two patterns more than any other geophysical signals, announced the ascent of Cotopaxi’s magma, although finally only a small quantity breached the surface.
In all likelihood little or no evidence of the 2015 restless period will be preserved in the geological record. We know from written chronicles (1534–1877) that Cotopaxi often had weeks to months of ramping up before unleashing VEI 3 or 4 eruptions, i.e. there were probably several poorly preserved 2015-sized like events, and therefore unrest has been poorly documented. In this recent case, scientists had the benefit of observing and analyzing the geophysical monitoring output during the entire episode and knowing what level of activity the volcano was at. But, monitoring scientists, just like the citizens of Ecuador, experienced the anxiety of pondering what could be the volcano’s next steps, i.e., the possible rapid intrusion of a new batch of volatile-rich magma or returning to calm. Fortunately, in this time around, the first scenario did not transpire. However, this training opportunity that we experienced could prove invaluable for when the next scenario is played out.
This work was supported by a grant from European Commission FP 7 program (ENV.2011.1.3.3-1; grant no: 282759; VUELCO). We would like to thank the IGEPN staff for keeping all monitoring operations at Cotopaxi volcano optimally functioning. Members of the IGEPN’s Volcanology group gave most of the talks and explanations of eruptions scenarios to authorities, community groups and wherever was necessary during the crisis. We acknowledge the VUELCO project for opportunities to share opinions about future eruptive crisis scenarios. Also, we are grateful for the support of the VDAP/USAID team during the crisis. The EPN, SENESCYT and SENPLADES provided funding for much of the instrumentation and daily operations. Support by JICA instrumentation and guidance is also noted. The Ecuadorian military provided overflights of Cotopaxi, while IGM provided ortophotos. The LMI project was instrumental in carrying out near real time petrologic monitoring. Thanks to Viviana Valverde for preparation of several figures. Recognition is given to the expressions of interest by STREVA project members on the societal implications of eruptive activity at Cotopaxi.
- Arias G (2015) Estudio de las Señales Sísmicas de Muy Largo Periodo del volcán Cotopaxi. Proyecto de Titulación, Facultad de Ciencias, Escuela Politécnica NacionalGoogle Scholar
- Arias G, Molina I, Ruiz M, Hernandez S, Alvarado A, Plain M, Mothes P, M Yépez, Hidalgo S, Barrington, C (2015) very long period seismicity accompanying increasing shallower activity at Cotopaxi Volcano. In Conference Paper No. S51D-2724, AGU Fall Meeting, San Francisco, 14–18 DecemberGoogle Scholar
- Bernard B, Battaglia J, Proaño A, Hidalgo S, Vásconez F, Hernandez S, Ruiz M (2016) Relationship between volcanic ash fallouts and seismic tremor: quantitative assessment of the 2015 eruptive period at Cotopaxi volcano, Ecuador. Bull Volcanol. doi: 10.1007/s00445-016-1077-5
- Cáceres B (2016) Dramatic reduction of Cotopaxi glaciers during the last volcano awakening 2015–2016. Conference: AGU Fall Meeting, San Francisco-Moscone Center. doi: 10.13140/RG.2.2.17483.80168
- Espín Bedón P, Mothes P, Montesdeoca M, Ruiz M, Alvarado A, Córdova M, Santamaria S (2016) Communication network of “Vigias” implemented at Cotopaxi Volcano, Ecuador, Abstract, Cities on Volcanoes-9, Puerto Varas, Chile, November, 2016Google Scholar
- Gaunt HE, Mothes P, Chadderton A, Lavallee Y (2015) Physical characteristics of conduit plug rocks during Vulcanian eruptions at Cotopaxi and Tungurahua volcanoes, Ecuador. Abstract, IUGG meeting, Prague-Czech Republic, June 2015.Google Scholar
- Gaunt EH, Bernard B, Hidalgo S, Proaño A, Wright H, Mothes P, Criollo E, Kueppers U (2016) Juvenile magma recognition and eruptive dynamics inferred from the analysis of ash time series: the 2015 reawakening of Cotopaxi volcano 328 October 2016. doi: 10.1016/j.jvolgeores.2016.10.013CrossRefGoogle Scholar
- Harlow DH, Power JA, Laguerta EP, Ambubuyog G, White RA, Hoblitt RP (1996) Precursory seismicity and forecasting of the June 15, 1991, eruption of Mount Pinatubo. Fire and Mud: Eruptions and Lahars of Mount Pinatubo, Philippines. University of Washington Press, Seattle, pp 285–306Google Scholar
- Hemmings B, Whitaker F, Gottsmann J, Hawes MC (2016) Non-eruptive ice-melt driven by internal heat at glaciated stratovolcanoes. Submitted to J Vol Geotherm ResGoogle Scholar
- Herring TA, King RW, Floyd MA, McClusky SC (2015) Introduction to GAMIT/GLOBK, Release 10.6. Department of Earth, Atmospheric, and Planetary Sciences, Massachusetts Institute of Technology, PSF: http://www-gpsg.mit.edu/~simon/gtgk/Intro_GG.pdf, 50p
- Hickey J, Gottsmann J, Mothes P (2015) Estimating volcanic deformation source parameters with a finite element inversion: The 2001–2002 unrest at Cotopaxi volcano, Ecuador. Journal of Geophysical Research: Solid Earth 120(3):1473–1486Google Scholar
- Hidalgo S, Bernard B, Battaglia B, Gaunt E, et al. (2016) Cotopaxi volcano’s unrest and eruptive activity in 2015: mild awakening after 73 years of quiescence. Geophys Res Abstracts Vol. 18, EGU2016-5043-1, 2016 EGU General Assembly, Viena-AustriaGoogle Scholar
- Jousset P, Budi-Santoso A, Jolly AD, Boichu M, Dwiyono S, Sumarti S, Hidayati S, Thierry P (2013) Signs of magma ascent in LP and VLP seismic events and link to degassing: an example from the 2010 explosive eruption at Merapi volcano, Indonesia. J Volcanol Geoth Res 261:171–192. doi: 10.1016/j.jvolgeores.2013.03.014CrossRefGoogle Scholar
- Kumagai H, Nakano M, Maeda T, Yepes H, Palacios P, Ruiz M, Yamashima T (2010) Broadband seismic monitoring of active volcanoes using deterministic and stochastic approaches. J Geophys Res: Solid Earth 115 (B8)Google Scholar
- Kumagai H, Mothes P, Ruiz M, Maeda Y (2015) An approach to source characterization of tremor signals associated with eruptions and lahars. Earth, Planets, and Space. 67:178, 67:178, doi: 10.1186/s40623-015-0349-1
- Lyons J, Segovia M, Ruiz M (2012) Reporte del Enjambre Sísmico en la Zona de Volcán de Cotopaxi—Mayo 2012. Internal report. Not published. IGEPN, Quito.Google Scholar
- Márquez M (2012) Caracterización de los sismos de muy largo periodo en el volcán Cotopaxi y sus implicaciones. Tesis de Grado, Carrera de Geofísica, Facultad de Ciencias Astronómicas y Geofísicas, Universidad Nacional de La Plata. ArgentinaGoogle Scholar
- Mothes P, Hall ML, Espín, PA, Vasconez F, Sierra D, Córdova M, Santamaría S, Andrade D (2016a) Mapa Regional de las Amenazas del Volcán Cotopaxi- Norte and Sur, scale 1:50,000, Instituto Geofísico and Instituto Geografico Militar, Quito http://www.igepn.edu.ec/mapas/mapas-volcan-cotopaxi.html
- Mothes PA, Nocquet JM, Jarrín Tamayo P, Morales Rivera AM, Lundgren PR, Yépez YM, Viracucha EG, Gaunt EH (2016b) Geodetic signature associated with unrest at Cotopaxi in 2015–2016: modeling of GPS data, a deep magma source, synchronous seismic swarms and petrologic constraints. Abstract, Cities on Volcanoes-9, Puerto Varas, Chile, November, 2016Google Scholar
- Mothes P, Hall ML, Andrade D, Yepes H, Pierson TC, Ruiz AG, Samaniego P (2004) Character, stratigraphy and magnitude of historical lahars of Cotopaxi volcano (Ecuador). Acta Vulcanol 16(1/2):1000–1023Google Scholar
- Mothes P, Lisowski M, Ruiz M, Ruiz G, Palacios P (2010) Borehole Tiltmeter and CGPS Response to VLP Seismic Events under Cotopaxi Volcano. Ecuador, Fall AGU, San Francisco AbstractGoogle Scholar
- Mothes PA, Vallance JW, Hall ML, Garrison JM (2015a) Cotopaxi’s most recent rhyolitic eruptions, 2800 y BP. In Conference Abstract, 26th IUGG General Assembly, PragueGoogle Scholar
- Newhall CG (2000) Volcano Warnings. In: Sigurdsson et al. (Eds) Encyclopedia of Volcanoes. San Diego, CA, pp 1185–1198Google Scholar
- Pistolesi M, Rosi M, Cioni R, Cashman KV, Rossotti A, Aguilera E (2012) Physical volcanology of the post–twelfth-century activity at Cotopaxi volcano, Ecuador: behavior of an andesitic central volcano. Geol Soc Am Bull 123(5–6):1193–1215Google Scholar
- Siebert L, Simkin T, Kimberly P (2010) Volcanoes of the World. Univ. of California Press and Smithsonian Institute. 551 pGoogle Scholar
- Sparks RSJ, Aspinall WP (2004) Volcanic activity: frontiers and challenges in forecasting, prediction and risk assessment. The State of the Planet: Frontiers and Challenges in Geophysics, Geophysical Monograph 150, IUGG Volume 19Google Scholar
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