Effusive silicic volcanism in the Central Andes: The Chao dacite and other young lavas of the Altiplano‐Puna Volcanic Complex

Abstract

The largest known Quaternary silicic lava body in the world is Cerro Chao in north Chile, a 14‐km‐long coulée with a volume of at least 26 km3. It is the largest of a group of several closely similar dacitic lavas erupted during a recent (< 100,000 year old) magmatic episode in the Altiplano‐Puna Volcanic Complex (APVC; 21‐24°S) of the Central Andean Volcanic Zone. The eruption of Chao proceeded in three phases. Phase 1 was explosive and produced ∼1 km3 of coarse, nonwelded dacitic pumice deposits and later block and ash flows that form an apron in front of the main lava body. Phase 2 was dominantly effusive and erupted ∼22.5 km3 of magma in the form of a composite couleé covering ∼53 km2 with a 400‐m‐high flow front and a small cone of poorly expanded pumice around the vent. The lava is homogeneous with rare flow banding and vesicular tops and selvages. Ogives (flow ridges) reaching heights of 30 m form prominent features on its surface. Phase 3 produced a 6‐km‐long, 3‐km‐wide flow that emanated from a collapsed dome. Ogives are subdued, and the lava is glassier than that produced in previous phases. All the Chao products are crystal‐rich high‐K dacites and rhyodacites with phenocrysts of plagioclase, quartz, hornblende, biotite, sphene, rare sanidine, and oxides. Phenocryst contents reach 40–60 vol % (vesicle free) in the main phase 2 lavas but are lower in the phase 1 (20–25%) and phase 3 (∼40%) lavas. Ovoid andesitic inclusions with vesicular interiors and chilled margins up to 10 cm are found in the later stages of phase 2 and compose up to 5% of the phase 3 lava. There is little evidence for preemptive zonation of the magma body in composition, temperature (∼840°C), ƒO2 (10−11), or water content, so we propose that eruption of the Chao complex was driven by intrusion of fresh, hot andesitic magma into a crystallizing and largely homogeneous body of dacitic magma. Morphological measurments suggest that the Chao lavas had internal plastic viscosities of 1010 to 1012Pa s, apparent viscosities of 109 Pa s, surface viscosities of 1015 to 1024 Pa s, and a yield strength of 8×105 Pa. These estimates indicate that Chao would have exhibited largely similar rheological properties to other silicic lava extrusions, notwithstanding its high phenocryst content. We suggest that Chao's anomalous size is a function of both the relatively steep local slope (20° to 3°) and the available volume of magma. The eruption duration for Chao's emplacement is thought to have been about 100 to 150 years, with maximum effusion rates of about 25 m3 s−1 for short periods. Four other lavas in the vicinity with volumes of ∼5 km3 closely resemble Chao and are probably comagmatic. The suite as a whole shares a petrologic and chemical similarity with the voluminous regional Tertiary to Pleistocene ignimbrites of the APVC and may be derived from a zone of silicic magmatism that is thought to have been active since the late Tertiary. Chao and the other young lavas may represent either the waning of this system or a new episode fueled by intrusio...

Morphology and stratigraphy of Serra Geral silicic lava flows in the northern segment of the Torres Trough, Paraná Igneous Province

“…In comparison, the dacitic Chao Flow in northern Chile has a volume of 26 km 3 . However, it is a single well-preserved porphyritic lava coulée that extends for 14 km and has a flow front ~400 m high (Silva et al 1994). The dacitic lavas of the SJP flowed uncommonly long distances (> 10 km) despite their acidic composition (66-70% SiO 2 ).…”

Origen y emplazamiento del Domo Tinto, volcán Guallatiri, Norte de Chile.

“…13), a feature that is very common in Pleistocene-Holocene andesitic and dacitic lavas of the Central Andes (e.g., the Chao Dacite; de Silva et al, 1994). An inclusion sample (#TD01) displays a dictytaxitic texture (Fig.…”

“…The slope. Eruption onto a flat surface, such as the bottom of a glacial valley, promoted the radial development of stacked lenticular lobes rather than the formation of a coulée or lava flow feature (e.g., de Silva et al, 1994). 5.…”

Emplacement of the Rocche Rosse rhyolite lava flow (Lipari, Aeolian Islands)

“…Pinkerton and Sparks 1978;Lipman and Banks 1987;Self et al 1997;Calvari and Pinkerton 1999;Cashman et al 1999;Kilburn 2000;Jerram 2002, Passey andBell 2007), such studies of more silicic lava flows are comparatively few (e.g. Fink 1983;de Silva et al 1994;Fujii and Nakada 1999;Uia et al 1999;Castro et al 2002;Harris et al 2002;Cioni and Funedda 2005;Tuffen et al 2013;Magnall et al 2016Magnall et al , 2017Latutrie et al 2017). This is due in part to a lack of observations of active flows.…”

“…Such structures are often evident and have been studied in viscous intermediate lava flows (e.g. Cerro Chao, ChileFink 1980b;de Silva et al 1994; Puy de Cliergue, France- Latutrie et al 2017;San Pietro, Sardinia-Cioni and Funedda 2005;Santiaguito, Guatemala-Harris et al 2002, and other rhyolitic lava flows worldwide (Fink 1980a(Fink , b 1983Manley and Fink 1987;Carn et al 2009;Lara 2009;Bernstein et al 2013;Pallister et al 2013;Tuffen et al 2013;Magnall et al 2017).…”