DOCSLIB.ORG

Supplementary Material

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text
Supplementary Material Supplementary Material In the following, the relevant data sets and test results, together with the corresponding figures, are shown for each volcano, together with a short comment on the volcano characteristics and the fit quality. The names adopted for the repose time fit parameters are exponential distribution: Weibull distribution: log-logistic distribution: Tupungatito year VEI year VEI year VEI Tupungatito Volcano is located in the high Andes east of Chile's capital 1829 2 1925 2 1961 2 Santiago, which is inhabited by six million people and by far Chile's 1835 2? 1946 2 1964 2 most important industrial and commercial centre. The volcano built up 1861 2 1958 2 1968 2 since Pleistocene times in the Nevado Sin Nombre Caldera (Siebert and 1889 2 1959 2 1980 2 Simkin, 2002), its recent activity consists of 18 smaller historical 1897 2 1959 2 1986 1 eruptions, which produced a total erupted volume of about 6 km³ 1901 2 1960 2 1987 2 (Sruoga et al., 1993). 1907 2 2 fit A t k d x0 p ²/DoF R KS-diff. AICc exp. 15.17±0.36 10.57±0.39 0.384 0.978 0.097 14.0 16± 0 9.97±0.27 0.442 0.974 0.095 14.0 WB 15.37±0.98 0.0970 0.9297 0.364 0.975 0.108 15.1 ±0.009 ±0.092 16± 0 0.1023 0.8811 0.356 0.975 0.126 13.3 ±0.003 ±0.039 log 15.04±0.51 6.881 1.494 0.445 0.976 0.134 17.1 ±0.470 ±0.097 16± 0 6.140 1.385 0.479 0.973 0.177 16.5 ±0.247 ±0.072 KS-threshold: 0.328 all fits pass the K-S-test The difference in AICc for fixed vs. fit A is minor for all distribution functions. The Weibull and exponential function give a slightly better fit than the log-logistic function, but the difference in AICc is not marked enough to significantly prefer these models. T [years] Exp_var Exp_const WB_var WB_const Log_var Log_const 0 0.0 0.0 0.0 0.0 0.0 0.0 1 9.0 9.5 8.2 7.8 5.5 5.1 2 17.2 18.2 15.7 15.0 10.6 9.9 5 37.7 39.4 34.6 33.3 23.3 21.9 10 61.2 63.3 57.0 55.1 38.9 36.8 20 84.9 86.5 81.1 79.2 58.1 55.3 50 99.1 99.3 98.3 97.7 80.6 78.1 100 100.0 100.0 100.0 99.9 91.0 89.3 200 100.0 100.0 100.0 100.0 96.3 95.3 500 100.0 100.0 100.0 100.0 99.0 98.5 1000 100.0 100.0 100.0 100.0 99.6 99.4 Maipo year VEI year VEI The ideally-shaped stratocone of Maipo Volcano is nested in the ~18 km diameter Diamante Caldera km that formed 450 ka BP (Sruoga et al., 2005). Seven historical 1826 2 1869 2 eruptions of VEI = 2 occurred over the past 200 years. Despite its location in the 1829 2? 1905 2 wider Santiago region (Región Metropolitana), the volcano and its surroundings are 1831 2 1908 2 developed for rustic tourism and therefore frequently visited. 1833 2 1912 2? 2 fit A t k d x0 p ²/DoF R KS-diff. AICc exp. 4.121±0.437 27.02±5.61 1.069 0.378 0.483 4.8 7± 0 11.41±1.33 1.797 0.076 0.609 22.8 WB fit cannot be performed 7± 0 0.1140 0.3281 0.550 0.503 0.388 -20.9 ±0.020 ±0.062 log 7.392±0.696 2.684 0.5523 0.491 0.722 0.342 -22.7 ±1.173 ±0.093 7± 0 3.190 0.5622 0.482 0.719 0.367 -24.7 ±0.807 ±0.091 KS-threshold: 0.486 all fits pass the KS-test except the exponential function for fixed A The Weibull function cannot be fit stably when A is a free parameter. In the case of the exponential, the AICc for fixed A is much worse than for variable A. For the log-logistic distribution, this difference is not so pronounced, but the fit is somewhat better for fixed A. The AICc of the exponential function (both for fit and variable A) is significantly worse than for the Weibull and log-logistic function, indicating that the exponential function provides a less satistfactory fit to the data. The log-logistic distribution performs better than the Weibull, which is still considerably better than the exponential distribution. T [years] Exp_var Exp_const WB_const Log_var Log_const 0 0 0 0 0 0 1 3.63 8.39 0.73 0.49 0.50 2 7.14 16.08 1.46 0.98 0.99 5 16.90 35.48 3.57 2.39 2.42 10 30.94 58.37 6.90 4.62 4.67 20 52.30 82.67 12.95 8.68 8.76 50 84.29 98.75 27.36 18.36 18.54 100 97.53 99.98 43.61 29.45 29.74 200 99.94 100 62.17 42.72 43.12 500 100 100 83.27 60.14 60.63 1000 100 100 93.07 71.10 71.61 Planchón-Peteroa year VEI year VEI year VEI Planchón-Peteroa is a compound volcanic edifice, where several interlaced 1660 >=3 1878 2 1960 1 calderas host the three volcanic centres Planchón, Peteroa, and Azufre, the 1751 2 1889 2 1962 1 latter of which collapsed at about 11.5 ka BP (Tormey et al., 1995). The 1762 4 1937 2 1967 1? largest historical eruption (VEI = 4) occurred in 1762, thereafter the volcano 1835 2 1938 2 1991 2 calmed to a series of smaller eruptions of VEI = 2, while the most recent eruptions during the past fifty years only reached a VEI of 1. The volcanic 1837 2 1959 1 1998 1 complex is flanked by a border crossing road to Argentina. 1860 2 As Planchón-Peteroa fails the test for independence, the analysis is repeated for eruptions after the year 1835. Still, the independence of successive eruptions cannot be ascertained, as the correlation coefficient points to a significant correlation (95% level of significance). Planchón-Peteroa is therefore excluded from the following analyses. Quizapu-Cerro Azul Historical eruptions of Cerro Azul took place through the parasite vent of Quizapu on its northern flank. The volcano is part of the larger Cerro Azul - Descabezado Grande - Resolana volcanic complex, year VEI characterised by several major stratovolcanoes and numerous small vents (Hildreth and Drake, 1992). 1846 2 Quizapu has produced one strong eruption in historical times, which is listed on the GVP-webpage as 1903 2 beginning in 1916 and lasting till 1932, although the major 9.5 km3 Plinian explosion took place in 1932. 1906 2 The influence of the exact onset date of this eruption on the statistical analysis is minor in this case, 1907 2 because it only switches the order of two repose times of 1-2 years and 16-17 years, respectively, which would rather smoothen the cumulative frequency plot and strengthen the stationary property of the data 1912 2 set. Since this VEI = 5+ eruption did not occur at the beginning of the eruption record but interspersed in 1913 2? a time interval with VEI = 2 eruptions, the record is considered to be complete and reliable. The VEI 5+ 1914 3 eruption followed the second strongest eruption of VEI = 3, suggesting that the volcano was 1916 5+ experiencing an episode of particularly fierce activity. The region around the volcano is intensely used: 1933 2 Major hydroelectrical power plants are constructed in the valley downstream of the volcano; several 1949 2? precious natural reserves attract a large number of tourists. Having been an ordinary border crossing to Argentina for a long time, the road connecting the Chilean metropole Talca with the Argentinian city of 1967 2? Malargüe via the Paso Pehuenche is currently upgraded and paved to become a major international hub. 2 fit A t k d x0 p ²/DoF R KS-diff. AICc exp. 7.264±0.36 15.36±1.12 0.552 0.853 0.323 34.4 10± 0 10.34±0.63 0.961 0.740 0.248 55.8 WB 8.316±1.20 0.08587 0.6569 0.344 0.874 0.181 24.6 ±0.0228 ±0.1106 10± 0 0.12336 0.5407 0.345 0.871 0.276 23.0 ±0.0083 ±0.0330 log 9.297±0.57 4.900 0.9772 0.394 0.897 0.175 27.3 ±0.818 ±0.0773 10± 0 4.058 0.9199 0.395 0.895 0.216 25.7 ±0.377 ±0.0594 KS-threshold: 0.410 all fits pass the KS-test The AICc is comparable for fixed vs. fit A in case of the Weibull and log-logistic distribution, but considerably worse for the exponential distribution. The exponential gives a less satisfactory fit that the Weibull; the log-logistic distribution, while not giving as good a fit as the Weibull distribution, still performs satisfactorily. T [years] Exp_var Exp_const WB_var WB_const Log_var Log_const 0 0.0 0.0 0.0 0.0 0.0 0.0 1 6.3 9.2 3.6 3.1 2.0 1.9 2 12.2 17.6 7.0 6.0 4.0 3.8 5 27.8 38.3 16.3 14.2 9.4 8.9 10 47.8 62.0 29.5 25.8 17.1 16.3 20 72.8 85.5 49.2 43.5 29.2 27.8 50 96.1 99.2 79.1 72.3 50.6 48.6 100 99.9 100.0 94.2 89.7 67.1 64.9 200 100.0 100.0 99.3 97.9 80.2 78.2 500 100.0 100.0 100.0 99.9 90.9 89.5 1000 100.0 100.0 100.0 100.0 95.2 94.2 Nevados de Chillán year VEI year VEI year VEI A series of major vents are aligned in an NNW-SSE trending direction at 1650 3? 1883 2? 1927 2? Nevados de Chillán, accompanied by several satellite vents (Dixon et al., 1999).
Load more

Recommended publications
  • Chile Relish Sleds Down the Fixed Ropes from High Camp to Low Camp
    106 T h e A l p i n e J o u r n A l 2 0 1 0 / 1 1 not stop for long before heading down the standard route to a point where we could put on skis at 4750m. From here we made a swift return to camp DEREK BUCKLE in less than an hour. We were looking forward to a quick descent to VBC but our difficulties were not over. We had not appreciated how hard it would be to lower the Chile Relish sleds down the fixed ropes from High Camp to Low Camp. Abseiling with the conjoined sleds was a tough challenge and it took three hours to get The 2010 Alpine Club expedition to Chile from 3500m to 2800m. Low Camp was enjoying the evening sun but the route to VBC was shrouded in low-lying mist. We had been anticipating a t was hot when we arrived in Santiago at the end of January, in marked smooth ski down gentle slopes to VBC. Instead we endured a tense descent Icontrast to the cold prevailing in the UK at the time. It was here that we met up with Carlos Bascou, our Chilean member who had worked hard on 74. Patrick Bird (left) planning our itinerary. He and Mike Soldner had conceived this expedi- and David Hamilton tion some years previously and had eventually decided on exploration of on the summit of Mt the mountains surrounding Tupungato from a base in the upper reaches Shinn. (David Hamilton) of the Rio Colorado.
    [Show full text]
  • University of Nevada, Reno a Study of Pleistocene Volcano Manantial
    University of Nevada, Reno A study of Pleistocene volcano Manantial Pelado, Chile: Unique access to a long history of primitive magmas in the thickened crust of the Southern Andes A thesis submitted in partial fulfillment of the requirements for the degree of Master of Science in Geology by Heather Winslow Dr. Philipp Ruprecht, Thesis Advisor May 2018 THE GRADUATE SCHOOL We recommend that the thesis prepared under our supervision by HEATHER WINSLOW Entitled A Study Of Pleistocene Volcano Manantial Pelado, Chile: Unique Access To A Long History Of Primitive Magmas In The Thickened Crust Of The Southern Andes be accepted in partial fulfillment of the requirements for the degree of MASTER OF SCIENCE Philipp Ruprecht, Ph.D., Advisor Wenrong Cao, Ph.D., Committee Member Adam Csank, Ph.D., Graduate School Representative David W. Zeh, Ph.D., Dean, Graduate School May, 2018 i ABSTRACT Textural and geochemical analysis of lavas and tephra from a poorly studied, glacially dissected, mafic, stratocone, Manantial Pelado, in the Southern Andean Volcanic Zone was collected to characterize the volcano’s petrogenesis and assess its primitive nature. Manantial Pelado lies within the transitional segment of the Southern Volcanic Zone (35.5°S) amidst thickened crust (~55 km) while surrounded by extensive silicic volcanism such as the Descabezado Grande-Cerro Azul Volcanic Complex. How mafic magmas reached the surface through thickened continental crust is a larger question at hand, but prior to addressing broader processes at work, initial geochemical characterization is necessary. Understanding the full extent of its primitive nature is crucial for broader insight of proximal vent interactions and relationships as well as insight towards magma genesis.
    [Show full text]
  • Sitting on Top of the World
    Notes from Mineralogy lecture on the chemistry and structure of various minerals (pyroxenes and amphiboles) that could crystallize from slowly cooling ers of lava flows and ash flows basalt magma. The different that built up the mountain. minerals reflect the changing In the regions exposed by conditions (temperature and erosion of these half-million- composition) in a magma chamber deep in the earth's year-old volcanoes, Dr. Wulff is crust. able to sample the lavas that poured out of the vents and built up the volcano, flow upon flow. “Sampling each flow allows us to evaluate the separate cycles of eruptive activity. By looking at the mineral compositions and whole- rock chemistry of the ancient PHOTO BY RYAN FILLOON Andrew Wulff and several undergraduate students take a break from sampling lavas, we can tell something about lava flows to plan the next traverse, under the imposing edifice of Volcan Cerro how the volcano has behaved over Azul in the Chilean Andes. time. This means we can make more accurate predictions of what will happen in the future,” he said. Two of his WKU undergraduate students are working with Chilean lava samples to determine whether SITTING ON TOP the volcanic complex is currently in a period of rapid growth or slower growth. “By compiling all these eruptive events into a composite OF THE WORLD history, we can get a good idea of how this complex behaves, and we can model individual eruptive B Y T O M M Y N E W T O N episodes. That’s a different approach from what most others are doing.” SOMEHOW IT SEEMS FITTING THAT Dr.
    [Show full text]
  • Report on Cartography in the Republic of Chile 2011 - 2015
    REPORT ON CARTOGRAPHY IN CHILE: 2011 - 2015 ARMY OF CHILE MILITARY GEOGRAPHIC INSTITUTE OF CHILE REPORT ON CARTOGRAPHY IN THE REPUBLIC OF CHILE 2011 - 2015 PRESENTED BY THE CHILEAN NATIONAL COMMITTEE OF THE INTERNATIONAL CARTOGRAPHIC ASSOCIATION AT THE SIXTEENTH GENERAL ASSEMBLY OF THE INTERNATIONAL CARTOGRAPHIC ASSOCIATION AUGUST 2015 1 REPORT ON CARTOGRAPHY IN CHILE: 2011 - 2015 CONTENTS Page Contents 2 1: CHILEAN NATIONAL COMMITTEE OF THE ICA 3 1.1. Introduction 3 1.2. Chilean ICA National Committee during 2011 - 2015 5 1.3. Chile and the International Cartographic Conferences of the ICA 6 2: MULTI-INSTITUTIONAL ACTIVITIES 6 2.1 National Spatial Data Infrastructure of Chile 6 2.2. Pan-American Institute for Geography and History – PAIGH 8 2.3. SSOT: Chilean Satellite 9 3: STATE AND PUBLIC INSTITUTIONS 10 3.1. Military Geographic Institute - IGM 10 3.2. Hydrographic and Oceanographic Service of the Chilean Navy – SHOA 12 3.3. Aero-Photogrammetric Service of the Air Force – SAF 14 3.4. Agriculture Ministry and Dependent Agencies 15 3.5. National Geological and Mining Service – SERNAGEOMIN 18 3.6. Other Government Ministries and Specialized Agencies 19 3.7. Regional and Local Government Bodies 21 4: ACADEMIC, EDUCATIONAL AND TRAINING SECTOR 21 4.1 Metropolitan Technological University – UTEM 21 4.2 Universities with Geosciences Courses 23 4.3 Military Polytechnic Academy 25 5: THE PRIVATE SECTOR 26 6: ACKNOWLEDGEMENTS AND ACRONYMS 28 ANNEX 1. List of SERNAGEOMIN Maps 29 ANNEX 2. Report from CENGEO (University of Talca) 37 2 REPORT ON CARTOGRAPHY IN CHILE: 2011 - 2015 PART ONE: CHILEAN NATIONAL COMMITTEE OF THE ICA 1.1: Introduction 1.1.1.
    [Show full text]
  • Glacier Runoff Variations Since 1955 in the Maipo River Basin
    https://doi.org/10.5194/tc-2019-233 Preprint. Discussion started: 5 November 2019 c Author(s) 2019. CC BY 4.0 License. Glacier runoff variations since 1955 in the Maipo River Basin, semiarid Andes of central Chile Álvaro Ayala1,2, David Farías-Barahona3, Matthias Huss1,2,4, Francesca Pellicciotti2,5, James McPhee6,7, Daniel Farinotti1,2 5 1Laboratory of Hydraulics, Hydrology and Glaciology (VAW), ETH Zurich, Zurich, 8093, Switzerland. 2Swiss Federal Institute for Forest, Snow and Landscape Research, Birmensdorf, 8903, Switzerland. 3Institut für Geographie, Friedrich-Alexander-Universität Erlangen-Nürnberg, Erlangen, 91058, Germany 4Department of Geosciences, University of Fribourg, Fribourg, 1700, Switzerland 5Department of Geography, Northumbria University, Newcastle, NE1 8ST, UK. 10 6Department of Civil Engineering, University of Chile, Santiago, 8370449, Chile. 7Advanced Mining Technology Centre (AMTC), University of Chile, Santiago, 8370451, Chile. Correspondence to: Alvaro Ayala ([email protected]), now at Centre for Advanced Studies in Arid Zones (CEAZA) Abstract (max 250 words). As glaciers adjust their size in response to climate variations, long-term changes in meltwater production can be expected, affecting the local availability of water resources. We investigate glacier runoff in the period 15 1955-2016 in the Maipo River Basin (4 843 km2), semiarid Andes of Chile. The basin contains more than 800 glaciers covering 378 km2 (inventoried in 2000). We model the mass balance and runoff contribution of 26 glaciers with the physically-oriented and fully-distributed TOPKAPI-ETH glacio-hydrological model, and extrapolate the results to the entire basin. TOPKAPI- ETH is run using several glaciological and meteorological datasets, and its results are evaluated against streamflow records, remotely-sensed snow cover and geodetic mass balances for the periods 1955-2000 and 2000-2013.
    [Show full text]
  • Volcán Tupungatito
    Volcán Tupungatito Región: Metropolitana Provincia: Cordillera Comuna: San José de Maipo Coordenadas: 33°23’S – 69°50’O Poblados más cercanos: El Alfalfal – los Maitenes – El Manzano Tipo de volcán: Estratovolcán Altura: 5603 m s.n.m. Diámetro basal: 7,5 km Área basal: 44 km2 Volumen estimado: 30 km3 Volcán Tupungatito. Vista desde el noroeste Última actividad: 1986 (Fotografía: Carolina Silva, SERNAGEOMIN) Última erupción mayor: 1959-1960 Ranking de riesgo 22 específico: Generalidades El volcán Tupungatito corresponde a un estratovolcán de corta vida (< 80 ka) y reducido volumen. Está emplazado en el extremo septentrional de la Zona Volcánica Sur de los Andes, a 75 km al este de Santiago. Forma parte de un grupo volcánico donde destacan los volcanes Tupungato y Nevado Sin Nombre, ambos inactivos. Durante su fase inicial este volcán registró una importante actividad efusiva, con generación de coladas de lava de hasta 18 km de alcance encauzadas en torno al valle del río Colorado, además de lahares, flujos piroclásticos y avalanchas de detritos de mediano alcance. Durante el Holoceno su actividad cambió a un estilo mixto (efusivo/explosivo), donde además de las coladas de lava se tiene registro de erupciones mayoritariamente vulcanianas. Este aumento en la actividad explosiva ha construido un sistema cratérico hacia la cumbre del volcán, el cual se localiza cercano a una depresión semi-circular de 4 km de diámetro rellena por un glaciar. En la actualidad exhibe actividad fumarólica intensa y permanente concentrada en uno de estos cráteres el cual, además, hospeda un lago ácido. Registro eruptivo Los registros de erupciones mencionan una veintena de eventos desde el siglo XVII, los que incluyen reactivaciones menores e incrementos en la actividad fumarólica.
    [Show full text]
  • Manual-Procedimiento Caída Cenizas Volcánicas
    MANUAL DE PROCEDIMIENTOS ANTE CAIDA DE CENIZAS VOLCANICAS Grupo de Estudio y Seguimiento de Volcanes Activos Proyecto “Exactas con la Sociedad” Facultad de Ciencias Exactas y Naturales – Universidad de Buenos Aires -2010- Autores Dr. Alberto Tomás Caselli Lic. María Laura Vélez Lic. Mariano Roberto Agusto Lic. María Laila Jover Colaboradores especiales Dra. Leonor Bonan Lic. Cintia Lorena Bengoa Srta. Diana Luz Sierra Lic. Ana María Fazio Prof. Patricia Castaño Dra. Ana Monasterio (EPROTEN) Ing. Agr. Carlos Prior (SENASA Zapala) Dr. Manuel Rivera (Coordinador de Emergencias Sanitarias Neuquén) Ing. Agr. Raúl Coppa (INTA Esquel) AGRADECIMIENTOS Los autores desean expresar su agradecimiento a todas las personas que brindaron información durante la recopilación realizada en las localidades en las que se hicieron entrevistas. En especial, queremos destacar la colaboración de los Intendentes de las municipalidades de Esquel, Trevelin, Corcovado, Los Antiguos y Caviahue-Copahue por la gran predisposición para responder nuestras consultas y contactarnos con el personal que actuó en la emergencia. En particular agradecemos al Intendente de la Municipalidad de Esquel Rafael Williams, al Secretario Gobierno Gustavo Lucero y colaboradores como Karina Araqué y Pablo Schulz, quienes se reunieron especialmente con nosotros y nos brindaron toda la información sobre la experiencia vivida. En la localidad de Trevelin, deseamos agradecer a Susana Thomas (Secretaria de Coordinación de Gabinete Municipalidad de Trevelin) y Alejandro Sabelli por la gran colaboración ofrecida y realizar los cuestionarios en la escuela publica, material de gran utilidad para acercarnos a la problemática de la población. Por otro lado, también agradecer al Intendente de la localidad de Corcovado, Héctor Diez y colaboradores, por la útil información brindada, en especial a lo referido a la región rural.
    [Show full text]
  • Late Pleistocene and Holocene Tephrochronology of Mendoza Province, Argentina
    O EOL GIC G A D D A E D C E I H C I L E O S F u n 2 d 6 la serena octubre 2015 ada en 19 Late Pleistocene and Holocene tephrochronology of Mendoza Province, Argentina Andres Bosch1; Charles R Stern*1 and Stella M. Moreiras2 1Department of Geological Sciences, University of Colorado, CB-399, Boulder, Colorado 80309-0399 USA 2CONICET,)Instituto)Argentino)de)Nivología,)Glaciología)y)Ciencias)Ambientales,)Mendoza,)CP5500,)Argentina Email: [email protected]! Abstract. Rhyolitic pyroclastic flows and tephra from the al., 1984) and Calabozos (300 and 150 ka; Hildreth et al., Pleistocene (450 ± 60 ka) eruption of the Laguna Diamante 1984) calderas have also been well documented. Here we caldera comprise the largest volume of pyroclastic material present preliminary results from a study in progress of late in northwest Mendoza Province. However, trace-element Pleistocene and Holocene tephra deposits in the province data indicate that 1-3 meter thick rhyolite tephra deposits, of Mendoza, Argentina. These results indicate that large which outcrop on both the southwest (Cacheuta) and late Pleistocene tephra deposits around the city of northeast (Borbollon) margins of the city of Mendoza, have Mendoza were not derived from the 450 ka Laguna an independent origin. These chemical data, and Diamante eruption, but from multiple younger eruptions of preliminary chronology, imply at least two different large some other source, and that numerous Holocene tephra late Pleistocene eruptions, both younger than that of the Diamante caldera, possibly of Tupungato volcano or the deposits outcropping along the Andean precordillera Tupungatito caldera.
    [Show full text]
  • Assessment of Exploitable Geothermal Resources Using Magmatic Heat Transfer Method, Maule Region, Southern Volcanic Zone, Chile
    GRC Transactions, Vol. 36, 2012 Assessment of Exploitable Geothermal Resources Using Magmatic Heat Transfer Method, Maule Region, Southern Volcanic Zone, Chile Diego Aravena and Alfredo Lahsen Departamento de Geología, Universidad de Chile, Centro de Excelencia en Geotermia de los Andes (CEGA) Keywords ment, and establishes a semi-logarithmic correlation between the Resource assessment, Maule, Southern Volcanic Zone, vol- resources and the volume of magma emplaced in the upper crust. canic arc, magmatic heat transfer, volcanic system, Monte Other heat-in-place techniques have been developed for estimat- Carlo, Chile ing geothermal resource size (e.g., Williams et al., 2008; Garg and Combs, 2010; 2011), but these methods are better suited for explored and identified geothermal systems. Abstract The mean calculated resources for the Maule region are ~1,400 MWe. These values are distributed between five main eruptive The Andean volcanic arc includes over 200 active strato- complexes with individual values that range from 177 to 392 volcanoes and at least 12 giant caldera systems. Nevertheless, MWe for 30 years. there is not a standard procedure for estimating geothermal resources associated with unexplored volcanic systems. The 1. Introduction study area corresponds to the main cordillera in the Maule re- gion, Chile, along the Southern Volcanic Zone (SVZ) between The Andean volcanic arc includes over 200 potentially active 34.8º and 36.5º S. The tectonic style and magma emplacement Quaternary volcanoes, and at least 12 giant caldera/ignimbrite model of this zone favors the occurrence of volcanic associated systems, occurring in four separate segments referred to as the geothermal systems, due to the presence of shallow magmatic Northern (ZVN; 2ºN-5ºS), Central (ZVC; 14-28ºS), Southern chambers and Cenozoic thrust faults that generate secondary (ZVS; 33-46ºS) and Austral (ZVA; 49-55ºS) Volcanic Zones.
    [Show full text]
  • Glacier Albedo Reduction and Drought Effects in the Extratropical Andes, 1986–2020
    Journal of Glaciology Glacier albedo reduction and drought effects in the extratropical Andes, 1986–2020 Thomas E. Shaw1,2 , Genesis Ulloa3, David Farías-Barahona4, 3 3,5 2,6 Article Rodrigo Fernandez , Jose M. Lattus and James McPhee 1 2 Cite this article: Shaw TE, Ulloa G, Farías- Swiss Federal Institute for Forest, Snow and Landscape Research (WSL), Birmensdorf, Switzerland; Advanced Barahona D, Fernandez R, Lattus JM, McPhee J Mining Technology Center, Universidad de Chile, Santiago, Chile; 3Department of Geology, Universidad de Chile, (2021). Glacier albedo reduction and drought Santiago, Chile; 4Institute für Geographie, Friedrich-Alexander-Universität Erlangen-Nürnberg, Erlangen, Germany; effects in the extratropical Andes, 1986–2020. 5SRGIS: Geología y Geomática Ltda, Santiago, Chile and 6Department of Civil Engineering, Universidad de Chile, – Journal of Glaciology 67(261), 158 169. https:// Santiago, Chile doi.org/10.1017/jog.2020.102 Received: 10 August 2020 Abstract Revised: 10 November 2020 Surface albedo typically dominates the mass balance of mountain glaciers, though long-term Accepted: 11 November 2020 First published online: 17 December 2020 trends and patterns of glacier albedo are seldom explored. We calculated broadband shortwave albedo for glaciers in the central Chilean Andes (33–34°S) using end-of-summer Landsat scenes Key words: between 1986 and 2020. We found a high inter-annual variability of glacier-wide albedo that is Albedo; Andes; climate; drought; glacier; largely a function of the glacier fractional snow-covered area and the total precipitation of the remote sensing preceding hydrological year (up to 69% of the inter-annual variance explained). Under the Author for correspondence: 2010–2020 ‘Mega Drought’ period, the mean albedo, regionally averaged ranging from ∼0.25– Thomas E.
    [Show full text]
  • Early British Ascents in the Andes (1831-1946)
    61 Early British Ascents in the Andes (1831-1946) Evelio Echevarria Plate 27 The purpose of this short contribution is to summarize those British ascents that took place in the Andes of South America, from 1831, year of the first British Andean ascent, until 1946. Most of these ascents are probably known to the readers of this journal, but some may be wholly new. A few ascents that for several reasons should no longer be included in this chronicle are discussed at the end. Readers who may feel inclined to study this survey are asked to maintain a proper sense of proportions and of time. A peak that 30 years ago demanded a long and frustrating approach may today be reached in a few hours of driving; a nOOm peak in S Chile has far more glaciation than a 5700m mountain of the Peruvian desert; what was considered to be a difficult ascent some seven decades ago may be regarded today as an easy one-day excursion for a hiker; and a mountain at present devoid of snow may have been snowclad until the end of last century. And so on. In the following list, names of climbers, peaks climbed (with height and location) and exact date of ascent are given whenever possible. A short comment is added when it may provide some useful or interesting additional information. Hall, 1831. Col Francis Hall joined French explorer Jean-Baptiste Boussing­ ault to attempt several peaks in the Ecuadorian Andes, but only one actual ascent took place, that of Pichincha (4791m), in the Cordillera Occidental.
    [Show full text]
  • USGS Open-File Report 2009-1133, V. 1.2, Table 3
    Table 3. (following pages). Spreadsheet of volcanoes of the world with eruption type assignments for each volcano. [Columns are as follows: A, Catalog of Active Volcanoes of the World (CAVW) volcano identification number; E, volcano name; F, country in which the volcano resides; H, volcano latitude; I, position north or south of the equator (N, north, S, south); K, volcano longitude; L, position east or west of the Greenwich Meridian (E, east, W, west); M, volcano elevation in meters above mean sea level; N, volcano type as defined in the Smithsonian database (Siebert and Simkin, 2002-9); P, eruption type for eruption source parameter assignment, as described in this document. An Excel spreadsheet of this table accompanies this document.] Volcanoes of the World with ESP, v 1.2.xls AE FHIKLMNP 1 NUMBER NAME LOCATION LATITUDE NS LONGITUDE EW ELEV TYPE ERUPTION TYPE 2 0100-01- West Eifel Volc Field Germany 50.17 N 6.85 E 600 Maars S0 3 0100-02- Chaîne des Puys France 45.775 N 2.97 E 1464 Cinder cones M0 4 0100-03- Olot Volc Field Spain 42.17 N 2.53 E 893 Pyroclastic cones M0 5 0100-04- Calatrava Volc Field Spain 38.87 N 4.02 W 1117 Pyroclastic cones M0 6 0101-001 Larderello Italy 43.25 N 10.87 E 500 Explosion craters S0 7 0101-003 Vulsini Italy 42.60 N 11.93 E 800 Caldera S0 8 0101-004 Alban Hills Italy 41.73 N 12.70 E 949 Caldera S0 9 0101-01= Campi Flegrei Italy 40.827 N 14.139 E 458 Caldera S0 10 0101-02= Vesuvius Italy 40.821 N 14.426 E 1281 Somma volcano S2 11 0101-03= Ischia Italy 40.73 N 13.897 E 789 Complex volcano S0 12 0101-041
    [Show full text]