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The Pleistocene (often colloquially referred to as the Ice Age) is the geological epoch which lasted from about 2,588,000 to 11,700 years ago, spanning the world's most recent period of repeated glaciations. The end of the Pleistocene corresponds with the end of the last glacial period and also with the end of the Paleolithic age used in archaeology.
Source: Wikipedia
Data Source: Smithsonian Institution Global Volcanism Program
Created: November 3, 2018
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South Harghita Mountains
Western Europe
Volcano type:
Lava dome(s)
Summit Elev: 1289 m
Latitude: 46.13°N
Longitude: 25.88°E
The Ciomadul lava-dome complex is the youngest volcanic center of the Carpathian-Pannonian region. Located at the SE end of the Calimani-Harghita Range, it consists of a dacitic dome complex formed about 500-700 ka. The dome complex is cut by twin craters, Mohos and St. Anna. The latest eruption, from St. Anna, produced subplinian airfall and pyroclastic-surge deposits that have been variously dated between about 10.7 and 42 ka. Pecskay et al. (2006) noted ages of 1.0-0.03 Ma. A number of samples from other South Harghita locations (Porcuhu, Cucu, Kapus, Pilisca, Balvanyos, Haramul Mare, and Koves Peak) had Quaternary dates.
Smithsonian Volcano Information

Persani Mountains
Western Europe
Volcano type:
Volcanic field
Summit Elev: 623 m
Latitude: 45.982°N
Longitude: 25.339°E
The Persani Mountains, an area that includes Pliocene-to-Pleistocene alkali basalts, are located south of the Calimani-Harghita Mountains in east-central Romania (Poka 1988). Bleheau et al. (1973) and Boccaletti et al. (1973) had also noted Pleistocene basalts in the area. Panaiotu et al. (2004) identified a number of volcanic features across a 22 x 8 km zone, finding that there were pulses of activity during 1.5-1.2 and 0.67-0.52 Ma.
Smithsonian Volcano Information

Apuseni Mountains
Western Europe
Volcano type:
Volcanic field
Summit Elev: 353 m
Latitude: 45.93°N
Longitude: 22.88°E
There are a number of locations south of the Apuseni Mountains in west-central Romania with deposits dated in the Quaternary. The Beritia lava dome (IAVCEI 1973) is located in an area of numerous alkali basalt vents of Pliocene-to-Pleistocene age (Bleahu et al. 1973, Poka 1988). Uroiu Hill, 15 km SE of Beritia, was dated by Pecskay (1995) at 1.6 +/- 0.1 Ma.
Smithsonian Volcano Information

Lucaret Basalts
Fissure vent
The Lucaret basalt plateau, located near Timisoara in west-central Romania about 35 km ENE of Timisoara, is thought to be early Pleistocene (Savu et al. 1994, Poka 1988). Bleahu et al. (1973) also noted Pleistocene basalts SE of Timisoara.

Bakony-Balaton Highland
Volcanic field
The Bakony-Balaton Highland Volcanic Field ia a large area of monogenetic Pliocene-to-Pleistocene basaltic shield volcanoes and cinder cones located around Lake Balaton in western Hungary (Bleahu et al. 1973, Poka 1988). The age of volcanism, as summarized by Kereszturi and Nemeth (2011), extended from ~7.94 to 2.29 Ma.

Little Hungarian Plain
The Little Hungarian Plain Volcanic Field (also called the Kemenesalja Hills) area in western Hungary contains a group of Pliocene-to-Pleistocene cones (Bleahu et al. 1973, Poka 1988). Martin et al. (2003) described it, and the Bakony-Balaton Highland field to the south, as an eroded phreatomagmatic field with remnants of nested maar complexes, multiple vent systems, and individual tuff rings.

Nograd-Southern Slovakia
The basaltic Nográd-Southern Slovakia volcanic field in north-central Hungary and southern Slovakia contains cones of Pliocene-to-Pleistocene age (Boccaletti et al. 1973, Poka 1988). The area is part of a larger volcanic field that straddles the Hungary-Czechoslovakia border. It is variously referred to as Northern Hungary-Southern Slovakia, or the Filakovo-Salgotarjan volcanics. Dating by Balogh et al. (1981 in Pecskay et al., 2006) gave dates of 0.4-2.2 Ma.

Central Slovakia
The Central Slovakia volcanic field consists of small basaltic shield volcanoes and cinder cones of Pliocene-to-Pleistocene age (Bleahu et al. 1973, IAVCEI 1973, Poka 1988). The SW part of the field is dominated by the Stiavnica stratovolcano, which is comprised of a large 18 x 22 km caldera, an extensive intrusive complex, and a resurgent horst with late-stage rhyolite. Based on stratigraphy (late Riss glacial stage), the Putikov vrsok cone of Stiavnica erupted about 130-140 ka (Simon and Halouzka, 1996). K-Ar dates from that scoria cone by Cherbyshev et al. (2013) were 390-460 ka, with the distal end of related lava flows slightly later.

Bruntal Volcanic Field
The Bruntal Volcanic Field in Moravia, west of Ostrava, contains many cinder cones and lava flows of Pliocene-to-Pleistocene age (IAVCEI 1973). Cajz et al. (2012) K-Ar dated lava from the Venusina volcano at 0.83 +/- 0.12 Ma.

Cheb Basin
An area of NW Bohemia near the border with Germany, known as the Czech Auvergne, contains small basaltic volcanoes of Miocene-to-Pleistocene age and world-renowned hot springs (Ager, 1980). Two cinder cones and a maar are found in the Cheb Basin area of the western Eger RIft; the Cheb Basin is an area of carbon dioxide dominated surface degassing in mofettes and mineral springs and active seismicity.

East Eifel Volcanic Field
Maar(s)
Activity at the East Eifel volcanic field began about 0.65-0.45 million years ago (Ma) with the formation of scoria cones, lava flows and tephra deposits. The Reiden volcanic complex at the western end produced a series of scoria cones, lava flows and lava domes from 0.45 to 0.35 Ma. Activity resumed around 0.215 Ma, continuing until 0.115 Ma, with the formation of scoria cones, maars and lava flows. The latest eruption, at the Laacher See maar, took place about 12,900 years ago (40Argon/39Argon age) and produced about 20 km3 of tephra (Schmincke et al., 2002).

Rodderberg
Pyroclastic cone
Rodderberg, in the Rodderberg Volcanic Complex (RVC), is a late Pleistocene cinder cone on the west side of the Rhine River. The complex itself consists of a circular depression with a diameter of about 600 m, a feature that is interpreted to be the remnant of a maar crater (Paulick et al., 2009). This field most likely represents a distal feature of the East Eifel Volcanic Field. The eruption of Rodderberg occurred in two phases. The first was phreatomagmatic, producing xenolith-rich, poorly sorted deposits. The second phase was dominated by Strombolian activity, resulting in xenolith-poor, thick and well-sorted coarse scoria deposits (Paulick et al., 2009). Geochemistry reveals the rocks erupted from the RVC to be leucitic nephelinite. The total erupted volume of material from the RVC eruption is estimated to be about 1.0x10^-2 km3 of magma and 2-3x10^-2 km3 of tephra - a rough order of magnitude estimate. The RVC deposits were previously dated at 26,000-27,000 years before present (IAVCEI 1973), but more recent thermoluminescence data placed the eruption at around 300 ka, during a glacial period in central Europe (Paulick et al., 2009).

Cofrentes
Longitude: 1.064°W
Mapped by Lopez-Ruiz et al. (2002) as part of the Pliocene-to-Pleistocene Gulf of Valencia volcanic province located west of Valencia, Spain.

Islas Columbretes
A group of islands in the Gulf of Valencia was mapped by Lopez-Ruiz et al. (2002) as Quaternary in age. The three largest islands are Illa Grossa, Illa Ferrera , and Illa Foradada.

Amiata
Italy
Lava dome(s)
Amiata is a lava dome complex located about 20 km NW of Lago di Bolsena in the southern Tuscany region of Italy. The trachydacitic domes and associated lava flows were erupted along regional ENE-WSW-trending faults. The largest of the domes is Monte Amiata (La Vetta), a compound lava dome with a trachytic lava flow that extends to the E. A massive viscous trachydacitic lava flow, 5 km long and 4 km wide, is part of the basal complex and extends from beneath the southern base of the Corno de Bellaria dome. Radiometric dates indicate a major eruptive episode about 300,000 years ago. No eruptive activity has occurred during the Holocene, but thermal activity, including cinnabar mineralization, continues at a producing geothermal field near the town of Bagnore, at the SW end of the dome complex.

Radicofani
Italy
Volcanic remnant
Summit Elev: m
Radicofani, a part of the Tuscan Magmatic Province located within the Sierra-Radicofani Graben, is a relatively small monogenetic volcano now represented by a volcanic neck (Peccerillo, 2005; Conticello et al., 2011). Although the original edifice was a cinder cone, it is highly dissected, leaving only lava flow remnants and scoria deposits east of Monte Amiata (Peccerillo, 2005; Conticello et al., 2011). Columnar jointing is present in the middle and lower portions of the neck and large lava blocks and bombs are scattered about within several kilometers (Conticello et al., 2011). The lavas are generally basaltic-andesitic to shoshonitic in composition (Conticello et al., 2011). The lavas of the upper and lower parts of the neck have been dated to about 1.3 Ma and 1.08-1.22 Ma ago, respectively (Conticello et al., 2011; Peccerillo, 2005).

Torre Alfina
Italy
Volcanic remnant
Summit Elev: m
Torre Alfina is a monogenetic volcano consisting of two volcanic necks and a lava flow several hundred meters long located SE of Monte Amiata (Peccerillo, 2005). Both blocky lava flows and smoother flows formed from lower viscosity lava crop out within a few kilometers of the volcano, and lapilli and scoria deposits surround the vent. Some lava tubes are also present in the eastern part of the lava field near the Paglia River canyon (Conticelli, 1998). These lavas are potassic alkaline olivine-latites and have been dated at 0.9-0.82 Ma (Conticelli, 1998; Peccerillo, 2005). Torre Alfina rocks contain a large number of crustal and mantle xenoliths (Conticello et al., 1998).

San Venanzo
Maar
The San Venanzo complex consists of the San Venanzo maar and the Pian di Celle tuff ring, both part of the Umbria-Latium ultra-alkaline district. The tuff ring is also associated with two spatter cones and a scoria cone. This complex of vents lies within the Tiber Valley Graben, where magmatism is believed to be a result of extension that began during the Pliocene (Stoppa, 1996). Early on, the eruption was explosive, producing pyroclastic flows and dry lapilli surges covering an area of about 0.15 km2; later eruptive behavior was dominated by lava flows. Block collapse and debris flows led to the formation of the steep inner crater walls. The tuffs of both San Venanzo and Pian di Celle are calcitic to carbonatitic in composition, and have been dated at about 265 +/- 3 ka (Stoppa, 1996; Stoppa and Sforna, 1995).

Acquasparta
Summit Elev: m
Acquasparta is characterized by monogenetic centers aligned N-S along a 10 km line. It's pyroclastic flow, fall, and surge deposits form a small plateau and are likely of phreatomagmatic origin. Ar/Ar dating of these products has produced an age of about 390 ka (Peccerillo, 2005).

Polino
Explosion crater(s)
Polino is made up of two small diatremes surrounded by layered tuffs and filled with breccia and carbonate-rich locks and lapilli (Pecerillo, 2005). It is classified as a carbonatite, the products of which consist of two facies: tuffisite and large carbonatite bombs. Both crustal and mantle lithics are also present within the welded tuff (Rosatelli et al., 2010). These deposits were Ar/Ar dated at about 246 ka (Peccerillo, 2005).

Cupaello
Pyroclastic cone
Cupaello is responsible for a 750-m-long lava flow that covers layers of pyroclastic material, including ash, breccias, lapilli, and scoria. These products were channelized and accumulated downslope of the volcanic edifice (Stoppa and Cundari, 1995). These pyroclastics are carbonatitic in composition, and yielded an Ar/Ar age of 639 ka (Peccerillo, 2005). However, Stoppa and Cundari (1995) list a date of about 491 +/- 3 ka. Structures within the pyroclastic layers indicate that the tuff could still deform plastically when covered by the lava, suggesting that both the explosive and effusive phases were part of the same eruption (Stoppa and Cundari, 1995).

Oricola-Carsoli
Pyroclastic cone(s)
Oricola-Carsoli, about 40 km SW of L'Aquila, is part of the Intra-Appenine Magmatic Province. Its mongenetic pyroclastic cones are composed of altered breccias, tuff, and surge and fall deposits. They are possibly hydrovolcanic in origin. These deposits were K-Ar dated at about 530 ka (Peccerillo, 2005).

Vico-Cimino Complex
Stratovolcano(es)
The Vico volcano is classified as part of the Roman Magmatic Province; however, the Cimino volcano that Vico partially overlies technically belongs to the Tuscan Magmatic Province, based on geochemical affinity (Peccerillo, 2005). The Monte Cimino trachytic lava dome complex was active from 1.35-0.94 Ma (Peccerillo, 2005). The PT Ignimbrite was erupted about 1.3 million years ago. The adjacent Vico central volcano and caldera was active during three periods from 0.4 to 0.15 Ma (Sollevanti, 1983; Peccerillo, 2005). Period 1 was dominated by pyroclastics and minor lava flows, Period 2 involved the emplacement of intermediate to felsic lavas that constructed the main cone. The post-caldera activity of Period 3 produced mafic lavas, scoria, and phreatomagamtic products. Vico also has a few post-caldera monogenetic centers, the largest of which is the Monte Venere cone inside the caldera (Peccerillo, 2005). Four ignimbrite-producing eruptions related to caldera formation took place from about 0.25-0.144 million years ago.

Sabatini Complex
Stratovolcano(es)
The Sabatini Volcanic Complex has no clearly delineated volcanic structure, but is a distribution of volcanic vents (Conticelli et al., 1997). The Sacrofano center in the eastern part of the complex and the Bacciano center in the west were active from 0.5 to 0.09 Ma (De Rita et al., 1983). Other smaller volcanic systems are Morlupo, Vigna di Valle, Trevignano, and Baccano (Conticelli et al., 1997). The Sacrofano and Bacciano centers dominate the five phases of the complex's eruptive history. The first two phases involved intense explosive activity at Sacrofano and Molupa (0.6-0.4 Ma), resulting in tuffs, ashes, and pyroclastic flows during the pre-Sacrofano Caldera stage. During the third phase, hydromagmatic eruptions formed the Sacrofano Caldera and minor lava flows occurred in the post-caldera stage. In the western sector, a stratovolcano and the Bracciano Caldera developed, along with fissure eruptions that produced flood lavas greater than 100 km3, air-fall tuffs, and surge deposits. Activity at small eruptive vents on the rims of the collapsed Bracciano and Sacrofano Calderas dominated the fourth phase, resulting in pyroclastics at Bracciano and parasitic cinder cones and lava flows at Sacrofano. Hyrdomagmatic activity localized between the two calderas, which produced tuff rings, cones, and maars, dominated the final phase (Conticelli et al., 1997).

Monti Ernici
The Monti Ernici volcanic field, also known as the Mid Latin Valley volcanic field, is a monogenetic center about 70 km SE of Rome. It consists of about 20 cinder cones, tuff cones, and associated lava flows and pyroclastic-flow deposits. The field was active from about 0.7 to 0.1 Ma (Peccerillo, 2005). Geochemically, the Ernici-Roccamonfina Province exhibits characteristics of both the Roman and Campanian Magmatic Provinces.

Roccamonfina
Stratovolcano
Roccamonfina is a large Pleistocene stratovolcano with numerous post-caldera cones within the summit caldera and on the flanks. The eruptive history consists of three main phases. The first stage built the main cone via lava flows and pyroclastics. The second stage is defined by large explosive eruptions, tuff deposits, and caldera collapse. The third stage formed the lava flows, domes, and scoria cones that exist on the volcanic edifice today. A report of a historical eruption in 269 BCE ("a flame shot up and burned for three days near Cales" (Stothers and Rampino, 1983)) is considered uncertain by Scandone and Principe (1986), who noted that the youngest products have been dated at 0.30 million years. Later work (Rouchon et al., 2008) dated summit caldera lava domes at 170-150,000 years ago. Peccerillo (2005) gives an age range of 0.58-0.1 Ma for Roccamonfina activity.

Monte Vulture
Stratovolcano
The isolated Monte Vulture is a stratovolcano with a summit caldera and a few parasitic cones that erupted lavas and pyroclastics covering 150 km2. Petrologically and geochemically distinct, it is therefore classified as its own magmatic province: the Lucanian Magmatic Province, in the Apulian Region (Peccerillo, 2005). The most recent volcanic activity formed two intra-caldera maars and involved explosive eruptions of carbonate-rich tuff, with the Lago Piccolo di Monticchio maar dated at 0.141 Ma (Peccerillo, 2005; Villa and Buettner, 2009). Capaldi et al. (1985) reported the youngest dated products from Vulture as 0.42 million years old. Peccerillo (2005) give an age range of 0.8-0.13 Ma for Vulture volcanics.

Ventotene
Stratovolcano(es)
Ventotene is a trachybasaltic to phonolitic stratovolcano with associated lava flows, domes, and pyroclastics (IAVCEI, 1973; Peccerillo, 2005). The mafic lava flows are cut by a caldera rim and overlain by pyroclastics. The nearby Santo Stefano island is an associated lava dome, also covered by pyroclastics. The pyroclastics are the products of both magmatic and hydrovolcanic processes, and contain lava lithic fragments and xenoliths (Peccerillio, 2005). Scandone (pers. comm.) gives 0.3 Ma as the youngest age for the Ventotene volcanics, but Peccerillo (2005) gives an age range of 0.8 to less than 0.13 Ma.

Pontine Islands
Lava dome(s)
The Pontine Islands are Plio-Pleistocene in age, ranging from 4.2-1.0 Ma (Scandone, 1987, pers. comm.; Peccerillo, 2005). The islands are mostly formed of Pliocene rhyolites and Pleistocene trachytes and alkaline rhyolites. Volcanic products also consist of obsidian lava flows, domes, dykes, breccias, and hydromagmatic products. The rhyolitic volcanic activity on Ponza occured between 4.2 and 3.0 Ma, followed by trachytic activity at about 1.0 Ma. The eruptive activity on Palmarola occured around 1.6 Ma (Peccerillo, 2005).

Logudoro
Plio-Pleistocene volcanic rocks ranging from 3.2 to 0.11 million years old are located in the Logudoro area of NW Sardinia (Beccaluva et al., 1977; Petteruti Lieberknecht et al., 2003; Peccerillo, 2005). Lustrino et al. (2007) gives an age of 2.4 to 0.1 Ma. These volcanics are generally of mafic composition, formed from monogenetic cinder and spatter cones, as well as lava flows (Peccerillo, 2005). Minor pyroclastics are also present. All together, the products of Logudoro cover about 500 km2 (Peccerillo, 2005).

Salina
Salina is made up of calc-alkaline basaltic to andesitic stratovolcanoes (Rivi, Capo, and Corvo), which are overlain by two andesitic cones (Monte Felci and Monte Porri), the latter of which erupted about 67 ka (Peccerillo, 2005). Monte Porri also underwent intense explosive activity, producing a series of tuffs that have also been identified on other nearby islands; these eruptions also produced lahars and pyroclastic surges (Guest et al., 2003). The final eruptive activity produced basaltic-dacitic-andesitic lava flows and a rhyolitic explosion crater (Pollara) (Peccerillo, 2005; Guest et al., 2003). Pollara Crater erupted about 13,000 years before present; the rest of the island is mid-upper Pleistocene, as old as 430 to 500 k.y. old (Keller, 1974; Peccerillo, 2005;Guest et al., 2003).

Filicudi
Filicudi was formed from the coalescence of eruptive centers that developed as part of a NW-SE elongated volcanic complex (Peccerillo, 2005; Guest et al., 2003). It's volcanic structures include basaltic to andesitic composite cones and dacitic domes, lava flows, and pyroclastics (Peccerillo, 2005). The Filicudi rocks also often contain igneous and metamorphic xenoliths (Peccerillo, 2005). Potassium-Argon dates of 0.170 and 0.166 million years were obtained by Capaldi et al. (1985), but Peccerillo (2005) gives a general age range of 440-40 ka. Tephrochronology indicates that the youngest eruptions occurred less than 35,000 years ago (Keller, 1989, pers. comm.). The Eruptive history is generally broken into four phases. The first (1.02 Ma) consisted of pyroclastic eruptions followed by lava flows. The second (390 ka) produced lava flows. The third is responsible for the construction of Fossa Felci, the main volcanic edifice on the island, and the production of basaltic andesitic lavas and pyroclastics. The fourth (40 ka) involved explosive activity from Fossa Felci, creating pumiceous pyroclastics (Guest et al., 2003).

Alicudi
Stratovolcano
Alicudi, in the Aeolian Island Arc, is a basaltic to andesitic stratovolcano containing a summit caldera, domes, and lava flows that formed over the course of three main stages in its eruptive history (Peccerillo, 2005). The first two stages involved basaltic to basaltic-andesitic lava flows and minor scoria and ash deposits, both followed by a summit collapse, the second of which formed the Dirittusu caldera (Peccerillo, 2005; Guest et al., 2003). Pyroclastic activity increased towards the end of the second stage (Guest et al., 2003). The third stage was dominated by andesite lava flows and the formation of domes within the summit crater and on the southeastern cone flank (Peccerillo, 2005). The youngest K-Ar date from Alicudi is 0.027-0.028 Ma, and the oldest, obtained from the lowest exposed rocks, is about 60-90 ka (Capaldi et al., 1985; Peccerillo, 2005; Guest et al., 2003).

Ustica
Ustica, the subaerial expression of a large submerged volcanic complex about 30 km wide, is formed mostly of lava flows, with minor hydrovolcanic products. Initial activity produced mostly pillow lavas, hyaloclastites, and breccias, having begun underwater. This was followed by effusive and hydromagmatic explosive activity, from two main volcanic centers: Monte Guardia dei Turchi (500 ka) and Monte Costa del Fallo (Peccerillo, 2005; Guest et al., 2003). These eruptions produced lavas, domes, basaltic scoria, pumice, and lapilli (Guest et al., 2003). This predominantly mafic activity was followed by a trachytic explosion and dome emplacement at about 424 ka (Peccerillo, 2005; Guest et al., 2003). One of the youngest eruptions on the island was a Surtseyan eruption, which produced extensive tuff deposits and formed the Falconiera pyroclastic cone (Guest et al., 2003). The volcanics on the island are middle Pleistocene, about 750-130 ka (Romano & Sturiale, 1971; Peccerillo, 2005; Guest et al., 2003).

Iblei
Shield?
Iblei consists of mostly submarine volcanics with some subaerial deposits; however, there is no clear volcanic edifice (Scandone, 1987, pers. comm.). The volcanic features consist mostly of monogenetic cones, maars, and lava flows of basaltic to andesitic composition; the older Pliocene submarine products are pillow lavas and hyaloclastites (Peccerillo, 2005). The youngest volcanic products are K-Ar dated at 1.7 Ma, but volcanism is believed to have taken place from 4.9 to 1.5 Ma (Capaldi et al., 1985; Peccerillo, 2005).

Linosa
Pyroclastic cone(s)
Linosa Island, in the Straight of Sicily graben system midway between Sicily and Tunisia, is the subaerial exposure of a large submarine volcano. The island contains several monogenetic hydrovolcanic eruptive centers, both effusive and Strombolian, as well cinder cones and lava flows dated to 1.06-0.53 Ma (Peccerillo, 2005). During this time, there were three main episodes of volcanism. The first phase developed hydromagmatic scoria cones and tuff rings of mafic composition. The second phase involved both effusive and explosive hydromagmatic activity, producing scoria and lava flows. The third phase produced basaltic lava flows, scoria deposits, and some hydromagmatic deposits, during which time the largest cones on the island formed (Peccerillo, 2005). Within each eruptive phase, hydromagmatic activity decreased with time, as lava flows helped reduce the islands erodability and limited the contact between craters and seawater (Guest et al., 2003).

Gaeta Bay Volcanic Field
Submarine
The Gaeta Bay Volcanic Field consists of a group of eight buried submarine volcanoes of Middle to Lower Pleistocene age (Torrente and Milia, 2013). This volcanism is generally characterized by thick lava flows and volcaniclastic deposits. The entire volcanic field is up to 1500 m thick. Volcanic activity in the Gaeta Bay and surrounding regions was largely fault bounded, where extension and subsidence controlled the emplacement and displacement of most of the volcanic centers (Torrente and Milia, 2013). These volcanic centers developed between 0.4 and 0.1 Ma. The oldest volcanic center is lower Pleistocene. The extension and volcanism responsible for the volcanic field migrated eastward with time, towards the Campi Flegrei (Torrente and Milia, 2013).

Sporades
Greece
Lava dome
Sporades, a small volcano on the island of Psathoura characterized by overlapping lava flows, is the northernmost Quaternary volcano in Greece. The volcano is also consistently and more often referred to by the name of the island, Psathoura (Koutsovitis et al., 2015; Pe-Piper and Piper, 2007). Koutsovitis et al. (2015) and Fytikas et al. (1984) give an age of 0.7 Ma for the Psathoura basalts. Other volcanism in the central and northern Aegean islands and the Western Thrace area of mainland Greece is of Oligocene to Pliocene age, with Quaternary volcanism being restricted to the southern Aegean arc (Fytikas et al., 1984). The volcanism is controlled by faulting along the North Aegean Trough, a westward extension of the North Anatolian Fault (Pe-Piper and Piper, 2007; Koutsovitis et al., 2015).

Volos-Atalanti
Greece
The Volos-Atalanti (also known as Volos-Evia) area contains a number of small monogenetic Pliocene to Pleistocene lava flows, cones, and domes. The largest lava outcropping, which originated from the Migoula cone, is about 0.2 km3 in volume and 6-7 km long (Innocenti et al., 2010). The volcanic products are generally basaltic trachyandesitic (Innocenti et al., 2010). The lava flows at Porphyrion and Microthivai date to about 1.6-1.3 Ma. The Toumbanos Hills lava dome, near Achilleion, dates to about 3.4-2.7 Ma. In the Atalanti channel, the cones and lava flows of the Likhades Islands date to about 0.5 Ma, as does a lava flow at Kammena Vourla on the Greek coast (Innocenti et al., 2010). K-Ar dates from Fytikas et al. (1984) range from 3.0-0.5 Ma. Volos-Evia is believed to lie on the westward extension of the North Anatolian Fault, rather than the Hellenic Arc (Innocenti et al., 2010).

Aegina
Greece
Aegina is part of the Saronic Gulf Volcanic Group, in the Hellenic Volcanic Arc. The complex consists of domes and lava flows erupted from effusive monogenetic centers with low eruption rates (0.4 km3/m.y. at Aegina) (D'Alessandro et al., 2008). Activity took place between 4.7 and 2.0 Ma, during the first part of which mostly basaltic-andesitic to rhyodacitic rocks were produced. The remaining 1 m.y. of its activity produced basaltic-andesitic rocks (D'Alessandro et al., 2008; Francalanci et al., 2007). Volcanic activity had ceased in the upper Pleistocene, but a low-temperature geothermal field presently exists (Keller, 1971; Francalanci et al., 2007).

Poros
Fissure vent
Poros consists of a small Pliocene to Pleistocene lava volcano erupted from fissures (IAVCEI, Keller 1982).

Antiparos
Pyroclastic cone(s)
Antiparos Island, positioned within the back-arc region of the South Aegean Volcanic Arc, contains a group of rhyolitic lava domes and pyroclastic cones with associated lava flows that are of Miocene to early Quaternary age (Pe-Piper and Piper, 2007; IAVCEI; Keller, 1982; Clapsopoulos, 1998). The domes are surrounded by tuffs containing obsidian particles and pumice, which are believed to be the result of subaqueous pyroclastic flows. The volcanic products are distributed over a total area of about 4.5 km2 (Clapsopoulos, 1998). K-Ar dates listed in Fytikas et al. (1984) range from 5.4 to 4.0 Ma.

Kos
Caldera(s)
The island of Kos is dominantly non-volcanic but contains Miocene to Pleistocene volcanic centers. The Kamari caldera is of mid-Pleistocene age and contains the 1.0-0.55 million-year-old, post-caldera Zini lava dome. The formation of a large caldera deposited the widespread Kos Plateau Tuff (erupted about 160,000 years ago), which blankets much of the western half of Kos and originated from a stratovolcano between Kos and Nisyros islands. The caldera dimensions are uncertain, but may extend as much as 20 km from Kefalos Bay in SW Kos Island to Nisyros Island. Remnants of the pre-eruption stratovolcano are preserved on the islets of Pachia and Pyrgousa and as submarine volcanic rocks on Nisyros. Kos was included in the Catalog of Active Volcanoes of the World (Georgalas, 1962) based on its geothermal activity. Several solfatara fields are present, including Vromotopos at Kefalos Isthmus on the western side of the island and a group of thermal areas at the eastern side of Kos. Thermal activity consists of weak hydrogen sulfide emission, sulfur deposits, and two hot springs along the southeastern coast.

Suphan Dagi
Turkey
Süphan Dagi is a basaltic-to-rhyolitic stratovolcano located immediately north of Lake Van with a glacial icecap on the summit. Andesitic-dacitic lava flows alternated with fluid basaltic flows, followed by construction of a large lava dome over the central vent. The flanks are dotted with numerous lava domes and pyroclastic cones erupted along radial and circumferential fissures, particularly on the N, S, and E sides. Voluminous basaltic lava flows traveled as far as 30 km from the summit. Although Yilmaz et al. (1998) reported that there had been a basaltic eruption about 10,000 years ago, Ozdemir and Gulec (2013) made no mention of any activity that recent; based on previous K-Ar studies and new Ar-Ar dating work, they found an activity range of 0.76-0.06 Ma. Dacitic and rhyolitic domes in the summit crater followed all lava flows and pyroclastic deposits from the main cone, with one dated at 64 +/- 14 ka. The 1.5-km-wide, low-rimmed Aygir Gölü maar was formed on the lower S flank, and represents the most recent activity (undated), characterized by a phreatomagamtic eruption and related deposits.

Girekol
Turkey
Shield
Girekol Tepe, a Pleistocene-to-Holocene, calc-alkaline to alkaline shield volcano, is located directly north of the NE arm of Lake Van and NE of the city of Ercis in eastern Anatolia (Yilmaz, 1990). Work by Lebedev at al. (2009) found no volcanic products younger than 0.36 +/- 0.06 Ma associated with Girekol.

Gölcük
Turkey
Caldera
Thick ignimbrite deposits are associated with formation of the Gölcük caldera, which was partially destroyed by a phreatoplinian eruption. The caldera was partially filled by lava domes and flows and then modified by maar formation during the last phase, which concluded with eruption of lava domes within the lake-filled maar. The volcano was initially thought to be Pliocene in age, but later work (Platevoet et al., 2008) has shown that much of the volcano's activity took place during the Pleistocene, and the latest eruption from lava domes took place about 24,000 years ago.

Kargapazari Dagi
Unknown
Kargapazari Dagi, located just north of the town of Pasinler and 35 km ENE of Erzurum (Ercan et al., 1993), was dated by Innocenti et al. (1982) around 8 Ma. However, Yilmaz (1990) identifies the area as Pliocene to Pleistocene based on dating by Nagao et al. (1989). Satellite imagery appears to show a half-caldera open to the NW with a dome in the center.

Arpacay
Latitude: 41°N
Arpacay is a Pliocene to mid-Pleistocene calc-alkaline to alkaline volcanic center (Yilmaz 1990).

Kisir Dagi
Unknown
Kisirdagi is a Miocene to Pleistocene volcanic center of calc-alkaline to alkaline composition (Yilmaz 1990).

Etrusk
As described by Oyan et al. (2010), the Pliocene Etrusk volcano is one of the major volcanic centers of eastern Anatolia, just NE of Lake Van. There is a ~5-km-wide horseshoe-shaped caldera near the center of the volcano, with the Pleistocene Karniyak scoria cone about 11 km away on the SW flank near the lake. K-Ar age determinations by Oyan et al (2010) indicate that the main volcanic edifice of Etrusk was formed between 4.3 and 3.9 Ma, ending with caldera collapse. Between ~1 and 0.43 Ma, basalts erupted from the SW flank, predominantly from a ~N-S extending fissure, as well as from Karniyarik hill and a maar-shaped volcanic center (Düzgeyikçukuru). Lebedev et al. (2009) noted that the youngest dated trachybasalt from Karniyarek was 0.36 +/- 0.06 Ma.

Karasu Rift
The Quaternary basalts of the Karasu Rift form a belt covering an area 94 km long and 12-25 km wide (as revealed by boreholes) between Fevzipasa and north of Revhanli in the northern section of the rift (Rojay et al., 2001). Located near the far NE corner of the Mediterranean Sea, some of the lava field extends into Syria. One especially dark fresh-looking are of lava flows just east of the city of Hassa covers an area of about 140 km2 over a N-S distance of 20 km, and includes the low Küçükak Tepesi crater. Those flows almost surrounded the older lavas of Büyükak Tepe. K-Ar age dating by Rojay et al. (2001) on new samples showed five preiods of volcanism between 1.6 and 0.05 Ma.

Ceyhan-Osmaniye
Latitude: 37°N
The Ceyhan-Osmaniye volcanic field, as summarized by Gursoy et al. (2003), includes basaltic eruptions from about 20 vents (Yurtmen et al., 2000) dated between 0.61 +/- 0.10 and 2.25 +/- 0.78 Ma (Arger et al., 2000). Outcrops and volcanic units along the Karatas Osmaniye Fault Zone NE of the Gulf of Iskenderum are described by a variety of names by different workers. Lava flows along the NW shoreline are identified by Gursoy et al. (2000) as the Botas Volcanics, while those just inland to the NE towards the city of Toprakkale are the Osmaniye Volcanics. The Osmaniye lava flows include a number of preserved vent locations, including the Delihalil Tepe tephra cone.

Keli Highland
Western Asia
This large volcanic plateau contains 35 small cones and extrusions, mostly andesite-dacite edifices (Lebedev, 2014, p.c.).

Akhuryan Valley
Western Asia
This group of six andesitic-dacitic cinder cones of lower to middle Pleistocene age was unnamed by IAVCEI (1973). Neill et al. (2013) sampled the Sepasar, Eznasar, and Kaputkogh cones in the "Cone Series" of the Akhuryan Valley. U-Pb dating of volcanic ash from a nearby archeological site gave an age of 1.8 Ma (Presnyakov et al., 2012).

Shamiram Plateau
Western Asia
A group of 13 cinder and lava cones and domes of Pliocene to mid-Pleistocene age are located in the Aragatz upland (IAVCEI 1973).

Unnamed
A group of four cinder cones and lava domes of Pliocene to upper Pleistocene age are found on the Vardenis upland (IAVCEI 1973).

Unnamed
A group of 11 cinder cones and lava cones and domes of Pliocene to mid-Pleistocene age are located in the Sjuni upland (IAVCEI 1973).

Dzau
Fissure vent
The Dzau (Java) volcanic center produced fissure eruptions of andesitic lavas between 200 and 100 ka (Chernyshev et al, 2002).

Borawli
Africa (northeastern) and Red Sea
This dome complex, one of several in Ethiopia named Borawli, consists of a group of rhyolitic lava domes on the floor of the southern Kali plain, NE of the town of Aisa Aita. A 1631 eruption (sometimes listed as 1627) attributed possibly to Amado dome (United Nations, 1973) was considered more likely to be from Dama Ali (Gouin, 1979). The southernmost lava flow dates from the Pleistocene, as K-Ar dated by Lahitte et al. (2003) around 0.49 Ma.

Oyma
Africa (northeastern) and Red Sea
Oyma is a complex stratovolcano with rhyolitic lava flows, domes, and pyroclastics, followed by formation of a 5-km-wide, 450-m-deep caldera. Oyma was age dated at around 0.5 million years ago (CNR-CNRS, 1973).

Didolli
Africa (northeastern) and Red Sea
Caldera
Included in Dubbi line of volcanoes which decrease in age northward (Mohr et al. 1976). Didolli is next volcano south of Omya which is dated at 0.5 million years ago (CNR-CNRS 1973).

Katahelu
Cone
Included in Dubbi line of volcanoes which decrease in age northward (Mohr et al. 1976). Katahelu is approx. 40 km S of Oyma which is dated at 0.5 million years ago (CNR-CNRS, 1973).

Ali Mela
Cone
Ali Mela Ale is included in Dubbi line of volcanoes which decrease in age northward (Mohr et al. 1976). Alimelali is next volcano SE of Oyma, which is dated at 0.5 million years ago (CNR-CNRS 1973).

Dawa Ale-Quarry
Longitude: 41°E
The Dada Ale silicic stratovolcano and caldera and the Quarry lava dome lie on opposite sides of the Dadar graben. These rhyolitic volcanoes, with potassium-argon dates of 0.62 and 0.65 million years, respectively, were orginally formed as a single volcanic structure that was dismantled by formation of the axial depression of the Dadar graben (Lahitte et al., 2003b).

Badi
A potassium-argon date of 0.29 million years was obtained from the silicic Badi volcano, located east of Dabbayra volcano (Lahitte et al., 2003b).

Gad Elu
Gad Elu is a 20-km-wide silicic stratovolcano with minor lava domes around the main cone and late-stage obsidian lava flows. Potassium-argon dates range from 1.46 to 0.38 million years (Lahitte et al., 2003a, 2003b).

Ela
The Ela silicic central volcano along the southern end of the Dadar graben was constructed by rhyolitic and trachtyic lavas capped by minor basaltic volcanism. The silicic stage was dated at about 0.52 million years (Lahitte et al., 2003a, 2003b).

Asgura
The silicic Asgura volcanic center lies SW of the central Manda Hararo cmplex and was potassium-argon dated at about 1.27 million years (Lahitte et al., 2003b).

Finini
The Finini silicic volcanic center lies NE of Kurub volcano and was potassium-argon dated at about 1.32 million years (Lahitte et al., 2003b).

Dalaha'ale
The silicic Dalaha'ale volcano is cut by a large caldera open to the NE, which has been referred to as Dalaha'ale and Asa Ale. Silicic activity here and at the adjacent Data Gabalti volcano was dated at about 1.52 to 0.95 million years and followed by fissural basaltic lavas from about 1.0 to 0.33 million years (Lahitte et al., 2003a).

Data Gabalti
The silicic Data Gabalti is located SW of the Manda-Inikar volcanic complex and ESE of Dalaha'ale volcano. Silicic activity at these two volcanoes was dated at about 1.52 to 0.95 million years and followed by fissural basaltic lavas from about 1.0 to 0.33 million years (Lahitte et al., 2003a).

Egersuwa
The Egersuwa silicic lava dome complex north of the NW end of the Manda Inakir has K-Ar dates ranging from 0.391 to 0.221 million years (Lahitte et al., 2003b).

Zikwala
Zikwala (Zuquala) is an isolated volcano west of the main Eithiopian Rift constructed of thick alkali-trachytic lava flows (Di Paola 1972). Potassium-Argon dates of 1.29 and 0.85 million years ago have been obtained (WoldeGabriel 1987, pers. comm.).

Ch'Ilalo
One of the largest volcanoes of the central Ethiopian Rift, Ch'Ilalo lies east of the main rift and contains a 6-km-wide summit caldera. Akali-trachytic lava flows occupy the caldera floor and a small basaltic flow is found on the NE rim (Di Paola 1972). A Potassium-Argon date of 1.76 million years ago has been obtained (WoldeGabriel 1987, pers. comm.).

Gademota Caldera
Caldera
Potassium-Argon date 1.27 million years ago (WoldeGabriel 1987, pers. comm.).

Duguna
Pleistocene in age (WoldeGabriel 1987, pers. comm.).

Chew Bahir
In the Chew Bahir basin along the Ethiopia-Kenya border cones of basaltic ejecta surrounded by very recent sediments. The volcanics are mapped as Quaternary (Davidson, 1983).

Undurer
Lahitte et al. (2003b) noted that "Despite poor constraints on timing of emplacement, Undurer and Babb-Olou volcanoes seem to have been more or less contemporaneous, erupting about 2 Myr ago...."

Babba'Olou
Lahitte et al. (2003b) noted that "Despite poor constraints on timing of emplacement, Undurer and Babba'Olou volcanoes seem to have been more or less contemporaneous, erupting about 2 Myr ago...."

Mabda
Lava dome
The Mabda complex, also called Dubbi Alto, is composed of rhyolitic lava domes (Wiart and Oppenheimer, 2005). The north flank has been partially covered by lava flows from Dubbi volcano, but it's relationship to that edifice is unknown. Although the age is also unknown, it's location between two Holocene volcanoes makes a Pleistocene age likely. In addition, there are fresher-looking cones and lava flows 9-12 km down the SSE flank (also possibly related to Dubbi) and a 32 km2 lava field 20 km SE (also possibly associated with Nabro).

Kilimanjaro
Africa (eastern)
Latitude: 3.07°S
Massive Kilimanjaro, Africa's highest mountain, consists of three large stratovolcanoes constructed along a NW-SE trend. The ice-capped summit towers 5,200 m above the surrounding plains. Activity at the older Shira cone, which forms the broad WNW shoulder, began during the Pliocene. The extensively dissected Pleistocene Mawenzi forms a prominent, sharp-topped peak on the upper ESE flank, dominated by a densely packed radial dike swarm. More than 250 satellitic cones occupy a rift zone to the NW and SE of Kibo, the central stratovolcano. A 2.4 x 3.6 km caldera gives the summit of Kibo an elongated, broad profile. Most of Kilimanjaro was constructed during the Pleistocene, but fumarolic activity is present within a group of youthful-looking nested summit craters. Widespread statements that the "most recent activity was about 200 years ago," sometimes referencing the central "ash pit" formation, are of unknown origin with no supporting evidence in geological or anthropological literature. Nonnotte et al. (2008) K-Ar dated caldera rim group lavas in the 170-274 ka range, and placed the most recent volcanism (formation of both the present summit crater, Inner Crater group lavas, and parasitic flank cones) around 150-200 ka.

Usangu Scarp Basalt
Africa (eastern)
Pyroclastic cone
Latitude: 8.624°S
A small basaltic tephra cone on the edge of the Usangu escarpment, overlooking the Usangu basin north of the Poroto Mountains, was considered by Ebinger et al. (1989) to be of probable Holocene age, based on lack of vegetative cover. A lava flow traveled westward away from the rift valley along the back-tilted flank of the rift. The exact location of this feature is uncertain and is not obvious at the mapped location using satellite imagery. More recent papers do not reference this location or provide age dates for the sample taken by Ebinger et al. (1989). Fontijn et al. (2012) considered the volcanic centers in the adjacent SW Usangu Basin area to be unrelated to the late Cenozoic stage of volcanism in the Rungwe Volcanic Province.

SW Usangu Basin
Africa (eastern)
Latitude: 8.75°S
A group of late-Pleistocene to Holocene phonolitic lava domes is located at the SW end of the Usangu Basin, NE of the Poroto Mountains. Vents of the SW Usangu Basin volcanic field are located along NNE-trending normal faults (Ebinger et al., 1989). However, Fontijn et al. (2012) considered the volcanic centers in this area, forming a phonolite dome field, to not be part of the late Cenozoic stage of volcanism in the Rungwe Volcanic Province; the most recent dated sample was 0.57 Ma.

Izumbwe-Mpoli
Two melanephelinite cones about 1.5 km apart, Izumbwe and Mpoli, are located ~18 km WNW of Ngozi caldera and just NW of Izumbwe village (Harkin, 1960). Basal lava flow trachyte units in the Songwe Basin were dated at 0.55 Ma (Ebinger et al., 1989). The youngest units in this area do not have age dates, but are covered with tephra from recent Rungwe and Ngozi eruptions.

Porr
Mohr and Wood (1976) map a Pliocene-Quaternary volcano in this location. Ochieng' et al. (1988) and Wilkinson (1988) map widely spaced Tertiary basaltic flows not associated with prominent volcanic centers. Smith (1991 pers. comm.) notes that the youthful features of the small volcanic cone Porr may indicate a Quaternary age.

Kulal
Shield
The elongated N-S trending Kulal shield volcano east of the south end of Lake Turkana is mostly Pliocene in age, with parasitic cinder cones of probable Pleistocene age (Ochieng' et al. 1988).

Asie
Shield
The Hawaiian-type Asie shield volcano is the youngest and NE-most of a group of en echelon shields east of Lake Turkana. Asie was constructed during the Pliocene and Pleistocene; late-stage activity formed a series of cones and maars, with the last eruptions occurring about 0.42 million years ago on the NW flank. (Charsley 1987a).

Huri
The 90 x 110 km Pliocene to Pleistocene Huri shield volcano is capped by cinder cones along a NNE-SSW trend. Some relatively uneroded cones in this arid region are over 1 million years old (Charsley 1987).

Bogoria
The late-Pleistocene Hannington formation consists of a broad shield volcano west of Lake Bogoria that has been cut by spectacular grid faults along the west margin of the Gregory Rift. Geysers on the west margin of Lake Bogoria may be of tectonic origin.

Kilombe Caldera
Pliocene-Pleistocene (Williams 1970).

Ol Doinyo Nyokie
Tuff cone
The late-Pleistocene Ol Doinyo Nyokie ignimbrite complex formed as a result of ash-flow fissure eruptions and ash flows erupted from a central vent, forming a dome-shaped tuff cone (Baker, 1975).

Gelai
Pleistocene shield volcano (Keller 1989, pers. comm.).

Ketumbeine
Activity at Ketumbeine volcano continued into the Pleistocene (Dawson, 1992).

Kerimasi
The carbonatitic volcano Kerimasi sits astride a major fault scarp of the eastern Gregory Rift and erupted during the last major episode of faulting 0.6-0.4 million years ago (Hay 1983).

Embagai
Included in a list of Quaternary volcanoes (Latter, 1975b).

Loolmalasin
Unknown
A lava flow, possibly from Loolmalasin, was K-Ar dated at about 1.19 million years (Dawson, 1992).

Olmoti
Latitude: 3°S
Included in a list of Quaternary volcanoes (Latter, 1975b); no additional information. Ages derived from both K-Ar and 40Ar/39Ar on lavas and ignimbrites presumably from Olmoti yielded ages of 1.10-1.85 Ma (McHenry et al., 2008).

Sadiman
Dawson (1992) considered the age of Sadiman volcano to be uncertain, with one source considering it to be Pleistocene and another obtaining a K-Ar age of 4.5 Ma. Clasts of Sadiman lavas are found in sediments dated to 1.7-2.0 million years.

Ngorongoro

Sultan Hamud-Simba
The lower Pleistocene Sultan Hamud-Simba volcanic cones and lava flows represent the beginning of volcanism that continued until the Recent to the SE in the Chyulu Hills (Saggerson 1963).

Burko
A K-Ar date of 0.97 +/- 0.03 million years was obtained from Burko volcano (Dawson, 1992).

Kwaraha

Hanang
Described as one of Pleistocene-Recent centers in the area, but not specifically described as Recent (Williams 1971).

Katete
This largely eroded Pleistocene volcano NE of Rungwe has never been studied systematically (Fontijn et al., 2012). A phonolite/trachyte sample from Katete was K-Ar dated by Ebinger et al. (1989) at 2.35 +/- 0.04 Ma.

Tukuyu
The Tukuyu shield volcano is thought to be made up of basaltic lavas, though Fontijn et al. (2012) also note that it has never been systematically studied. The town of Tukuyu is built upon thsi volcano. Dating by Ebinger et al. (1989) using K-Ar and by Ivanov et al. (1999) identified three lava ages between 2.12 +/- 0.04 and 1.34 +/- 0.02 Ma.

Lenderut
Mapped as Pleistocene (Guth and Wood, 2014).

Shombole
Cone
Mapped as Pleistocene (Guth and Wood, 2014).

Mikeno
Africa (central)
The eroded Pliocene to Pleistocene Mikeno volcano is located west of the crest of the Virunga Mountains. Potassium-Argon dates of 0.5 million years ago have been obtained for its latest stage of activity (Krafft 1990).

Sabinyo
Africa (central)
Extensive erosion has carved five peaks into the summit of the Pliocene to Pleistocene Sabinyo volcano. Potassium-Argon dates of 0.14 and 0.09 million years ago have been obtained from lava flows.

Sao Tome
Africa (western)
Sao Tome is a roughly conical island in the Gulf of Guinea that rises from a depth of 3,000 m below sea level. The S and W parts of the island are more dissected, and dramatic phonolitic and trachytic spines rise vertically out of the rain forest. Most of the lavas erupted over the last million years are basaltic in composition. Argon isotope dating reported by Barfod and Fitton (2014) showed that the most recent activity was 0.036 +/- 0.004 Ma, following frequent eruptions over much of the Pleistocene.

Manengouba
Africa (western)
The Manengouba volcanic complex rises to 2411 m across the Tombel Graben from Mount Cameroon. Growth of the initial Manengouba shield volcano during the early Pleistocene was followed by growth of the Eboga stratovolcano. The subsequent Elengoum extrusive complex consists of trachytic pyroclastic flows and trachyandesitic to trachytic lava domes, and magma withdrawal associated with these eruptions was linked to formation of the 4-km-wide Eboga caldera. Renewed eruptions within the caldera and on its flanks produced about one hundred pyroclastic cones and three maar volcanoes during the latest stage of activity at Manengouba that were dated between about 0.45 and 0.11 Ma.

Ngaoundere Plateau
Africa (western)
The Ngaoundere volcanic field is located within a larger late-Miocene region of plateau basalts, plug domes and a single large basanitic-to-trachytic stratovolcano, Nganha. Quaternary volcanism is situated east of Ngaoundere and Wakwa, and consists of scoria cones and lava flows, maars, and tuff cones. A single Potassium-Argon date of 0.9 million years ago has been obtained from a lava flow east of Wakwa, although some volcanoes are possibly of Holocene age (Vincent 1992, pers. comm.). The most recent eruptive activity originated from a chain of cinder cones aligned in a WNW-ESE direction.

Biu Plateau
The Biu Plateau in NE Nigeria is composed of basaltic lava flows. A large number of recent cinder cones with well-defined craters are aligned in a NNW-SSE direction over a distance of 50 km. The cinder cones and lava flows often contain abundant peridotite xenoliths. Work in this area has been inconsistent and infrequent. Age dates (K-Ar) were reported by Lar and others (2013; citing Baudin, 1991) as being in the 5-1.4 Ma range. Fitton and Dunlop (1985) presented K-Ar ages of 5.20 +/- 0.33 Ma for a basalt 24 km S of the town of Biu near the base of the plateau, and 0.84 +/- 0.09 Ma for a basanite on the north end of the plateau; neither roadside sample was clearly identified with a specific cone. Obaje (2009) describes the chronology of the Biu Plateau as "well controlled by radiometric dating" with plateau basalts in the 7-5 Ma range and Quaternary basalts less than 1 Ma; no citations are provided. A pollen record from Lake Tila (Salzmann, 2000) spanned the entire Holocene; however, adjacent graph scales showing age (in ka BP) and core depth terminating at 840 cm have apparently been misunderstood, resulting in Salzmann being cited in some places as indicating volcanism 840,000 years ago.

Jos Plateau
Longitude: 9°E
Volcanic features on the Jos Plateau include domes, single vents, and clusters of 3-4 cones aligned mainly NW-SE (Lar and others, 2013). Preliminary K-Ar dating of volcanci features reported by Lar and others (2013) showed an age range of 2.5-1.34 Ma.

Kumba Volcanic Field
Maar(s)
Volcanic field SW of Tombel Graben and NNE of Mount Cameroon (within rectangular area of 4°48'15"N, 9°30'E and 4°24'15"N, 9°5'E). This area is known for the maar lakes Barombe Mbo, Barombi Koto, and Mboandong.

Haruj
Africa (northern)
The extensive Plio-Pleistocene Haruj volcanic field covers a broad 45,000 km2 area in central Libya with very well-preserved basaltic scoria cones, lava flows, and explosion craters (Liegeois et al., 2005). The youngest lava flows of the Haruj field (also known as Al-Haruj al Aswad or Djebel Haroudj) were considered by Klitzsch (1968) to be Holocene in age and are located at the northern side of the field, but K-Ar ages generally range from 6 to 0.4 Ma (Liegeois et al., 2005). The field contains about 150 volcanoes, 30 of which are small shield volcanoes with heights between 100 and 400 m. The volcanics are located along the SE extension of the Hon graben system of late Cretaceous to Tertiary age, near the intersection of the Paleozoic southern Haruj uplift and the western edge of the Mesozoic Tibesti-Sirte uplift.

Waw an Namous
Africa (northern)
The isolated Waw an Namous (also spelled Wau-en-Namus or Uaw en Namus) lies in the Sahara desert of south-central Libya, south of the Haruj volcanic field. A 4-km-wide, 100-m-deep caldera contains the Waw an Namous post-caldera scoria cone. An apron of dark basaltic tephra extends 10-20 km around the caldera in stark contrast to the light-colored desert sand prominent in satellite views. Three small salt lakes of variable color contribute to the name of the volcano, which means "Oasis of Mosquitoes." The youthful appearance of the central cone has suggested it may be as young as a few thousand years, although the arid climate may mask its actual age. Yellow sulfur deposits are found in the 150-m-wide crater. Other basaltic lava flows occur several tens of kilometers NW of the volcano.

Tin Taralle Volcanic Field
Africa (northern)
The Tin Taralle volcanic field was erupted through Precambrian basement rocks of the Tuareg shield in the southern Aïr region of Niger. The latest dated rocks are of Pleistocene age (Liegeois et al., 2005).

Cap-Vert
Longitude: 17.4°W
Volcanism on the Cap-Vert Peninsula took place in five episodes from the Oligocene to the Pleistocene, ending about 600,000 years ago. The volcanic field covers an area of about 100 km2 on the peninsula hosting the capital city of Dakar.

In Teria Volcanic Field
Tuff ring(s)
The In-Teria volcanic field, which covers an area of about 100 km2, consists of about 20 explosion craters that produced tuff rings and xenolith-rich porphyritic melilititic rocks (Liegeois et al., 2005). Lava blocks and lapilli are found within the tuffs, which may be phreatomagmatic in origin (Dautria et al., 1992). The fresh-looking morphology of some tuff rings suggests a Quaternary age (Dautria et al., 1992). Liegeois et al. (2005) suggest In-Teria may be Holocene, but are uncertain.

Oulmes Volcanic Field
Longitude: 6°W
The alkaline Olmès volcanic field covers an area of 20 x 70 km in the Middle Atlas Range of Morocco. The volcanic field was active during the Pliocene and Pleistocene, with K-Ar dates of 0.9-0.31 million years (Liegeois et al., 2005).

Azrou Volcanic Field
Longitude: 5.17°W
The Azrou volcanic field in the Middle Atlas Range of Morocco covers an area of about 1500 km2.

Rekkame Volcanic Field
Explosion crater(s)
The youngest rocks of the Rekkame volcanic field were K-Ar dated at 1.4 million years (Liegeois et al., 2005).

Oujda Volcanic Field
Includes more than 20 older Quaternary volcanoes (IAVCEI).

Mrit-Ment Volcanic Field

Berguent Volcanic Field

Chott Tigri Volcanic Field

Nemours-Nedroma
Longitude: 2°W
An age of 2.1 million years was obtained from this part of the Oranie Volcanic Field, a 2000 km2 field located along the Mediterranean coast of NW Algeria (Coulon et al., 2002; Liegeois et al., 2005). It is not known if younger rocks are present in this part of the field. Maury et al. (2000) gives ages of 0.8 to 3.9 Ma for the whole Oranie Volcanic Field. The volcanic products associated with this field are generally alkaline basalts; mantle xenoliths are also present within the volcanics (Maury et al., 2000; Liegeois et al., 2005).

Tafna Beni Saf
Alkaline volcanism continued into the Pleistocene in the Tafna Beni Saf (2.7-1.4 Ma) and Aïn Temouchent (1.28-0.82 Ma) areas along the Mediterranean Sea coast of NW Algeria (Coulon et al., 2002). This volcano is a member of the Neogene-Pleistocene Oranie Volcanic Field, which covers an area of about 2000 km2 and has a total volume of about 200 km3. The volcanic products generally consist of alkaline basalts, and mantle xenoliths are also present (Doblas et al., 2007; Maury et al., 2000; Liegeois et al., 2005).

Gharyan Volcanic Field
Latitude: 32°N
The Gharyan volcanic field is about 3000 km2 in area, but its volcanic structures and products, which include a lava plateau, phonolite domes, and younger small volcanic centers, are relatively thin, at only 350 km3 in volume (Liegeois et al., 2005). Potassium-Argon ages of the youngest volcanics range from 1-12 Ma (Almond, 1974; Liegeois et al., 2005). These volcanic centers are generally basanitic and contain abundant lherzolitic xenoliths (Liegeois et al., 2005).

Tarso Emi Chi
Tarso Emi Chi forms a SSW-NNE trending massif capped by Quaternary basalts (Geze et al. 1959).

Tarso Ahon
Tarso Ahon forms an elongated ridge 100 km long running NNW from Emi Koussi that is capped by Quaternary basalts from well-preserved vents (Geze et al., 1959).

Unnamed
Middle East (western)
Mid-Pleistocene (IAVCEI 1973).

Middle East (western)
Cone(s)
Group of 11 volcanoes last active in mid-upper Pleistocene (IAVCEI)

Middle East (western)
Cone(s)
Group of 7 volcanoes last active in mid-upper Pleistocene (IAVCEI)

Cone(s)
Group of 8 mid-Pleistocene volcanoes (IAVCEI 1973).

Group of 34 mid-Pleistocene volcanoes (IAVCEI 1973).

Jabal al Qiranah
Jabal al Qiranah lies in central Jordan, about halfway in between the city of Ma'an in southern Jordan and the Dead Sea. Basaltic lava from Jabal al Qiranah overlies middle Pleistocene fluviatile gravels, which yielded many Acheulian implements (Bender, 1975).

Kuh-e Ayyub Ansar
Lava dome
Two volcanic centers near Takab noted by Boccaletti (1976-77) may be the same features identified in IAVCEI (1973) to the SE of Sahand volcano, though located about a degree of latitude further south. The northern-most feature, Kuh-e Ayyub Ansar, appears to be a dome (about 3 x 5 km) in satellite imagery. A second hill about 20 km ESE may be a resistant outcrop of a lava flow, a situation seen in other parts of Iran.

Bijar Volcanic Field
The Bijar volcanic field of a cluster of Miocene dacitic and rhyolitic lava domes and a group of Pleistocene (Potassium-Argon dates 1.3-0.5 million years ago) alkaline cinder and spatter cones and two rhyolitic lava domes (Boccaletti et al. 1976-77).

Harrat Hutaymah
Middle East (southern)
Harrat Hutaymah is a Quaternary alkali basalt volcanic field that is rich in tuff cones and ultramafic xenoliths (Thornber, 1990). It lies NE of the trend of the main lava fields of Saudi Arabia and is one of the smaller fields. One K-Ar date of 1.80 +/- 0.05 was obtained from a lava flow cut by a tuff ring.

Jibal al Haylah
Middle East (southern)
This isolated cone about 20 km E of late lava flows from the Harrat al Birk field was dated as Pleistocene (0.18-0.25 Ma) by Coleman et al. (1983). However, Brown et al. (1989) noted that those samples were from a basal flow, so the youthful-looking cone could be much more recent.

Jabal Baqarah
Middle East (southern)
This isolated cone surrounded by lava flows about 18 km NE of the southern part of the Harrat al Birk field was considered to be similar in age to Jibal Haylah (54 km N), dated as Pleistocene by Coleman et al. (1983).

Qal'eh Hasan Ali
Middle East (eastern)
Maar(s)
The Qal'eh Hasan Ali volcanic field in SE Iran contains 14 maars of late Quaternary age, which were erupted through desert alluvium, granodioritic rocks, and Eocene volcanics in an area several hundred kilometers away from the closest Quaternary volcanoes. The maars, which produced tephritic pyroclastic deposits, have diameters ranging from 150 to 1200 m. The largest, known as Great Crater, is 1.2 km wide and 200-300 m deep. Ar-Ar dating of phlogopite in volcanic bomb samples from Great Crater gave ages of 112-119 ka (Pang and others, 2015).

Dacht-i-Navar Group
Middle East (eastern)
The Dacht-i-Navar volcanic field is a group of 15 trachyandesitic lava domes located in west-central Afghanistan SW of Kabul. The domes lie along the southern margin of Dacht-i-Navar. The age of the volcanoes is not known precisely; they were tentatively considered to be of Pleistocene age (Lapparent et al., 1965) and were listed as Recent by Bordet (International Association of Volcanology and Chemistry of the Earth's Interior, 1973).

Vakak Group
Middle East (eastern)
The Vakak Group (also spelled Wakak) consists of 18 dacitic and trachytic volcanoes located WSW of Kabul. It is the northernmost of a group of small volcanic fields in the Ghanzi region and consists of endogenous lava domes, one of which occupies an old caldera. The age of the volcanoes is not known precisely; they were tentatively considered to be of Pleistocene age (Lapparent et al., 1965) and were listed as Recent by Bordet (International Association of Volcanology and Chemistry of the Earth's Interior, 1973).

Gandom Beryan
Previously identified as an unnamed area with two small Quaternary centers (IAVCEI 1973), this location corresponds to the lava plateau (480 km2) on the edge of the Dasht-e Lut (Lut desert) of Iran named Gandom Beryan (meaning "Scorched Wheat" in Persian). Also known as Gandom-e Beryan or Rig-e Soukhteh, it is located 80 km N of Shahdad city. Some small cinder cones are present, but the source of the extensive basalt flows is not certain. It has been touted as the "Hottest place on Earth" with reported temperatures as high as 67C in the summer. Ar-Ar dating (Walker et al., 2009) of basalts from three locations in the lava field ranged from about 2.15 to 2.80 Ma.

Dehaj-Meduk
Dehaj-Meduk is a Quaternary andesitic volcano group with perfectly preserved volcanic cones (Catalog of Active Volcanoes of the World, Jung et al. 1976).

Shahsavaran
A group of small perfectly preserved Quaternary lava cones covering an area of 60 x 120 km west of Bazman volcano have produced viscous basaltic lava flows (Catalog of Active Volcanoes of the World, Girod and Conrad 1975).

Sultan
The lower Pleistocene Sultan volcano group consists of six volcanoes along a 76-km length of an E-W fault (IAVCEI 1973).

Zardolou Group
Six or seven Quaternary lava domes (IAVCEI 1973).

Loman Volcano Group
Four Quaternary lava domes (IAVCEI 1973).

East Neh
Walker et al. (2009) dated basalts along the East Neh fault at 1.45-1.75, 1.69-1.79, and 4.71-4.91 Ma. Volcanic deposits are strung out along perhaps 50 km on either side of the fault.

Moheli Island
Indian Ocean (western)
The Pliocene-to-Pleistocene Moheli Island, also known as Mwali, was constructed by eruptions along a NW-SE rift zone. A renewal of activity during the late Pleistocene produced very fresh lava flows and well-preserved cinder cones (Strong, 1972; Krafft, 1983).

Anjouan Island
Indian Ocean (western)
The large, triangular-shaped island of Anjouan is the dissected remnant of a large shield volcano. Formation of the N'Tingui shield volcano was followed by fissure eruptions in three directions of Pleistocene age. A long interval of erosion was followed by the eruption of lava flows that filled deep valleys and flooded coastal areas.

Piton des Nieges
Indian Ocean (western)
The massive Piton des Nieges shield volcano occupies the NW side of Reunion Island. The now 3070-m-high volcano emerged from the sea about 2.1 million years ago, beginning construction of a basaltic subaerial shield volcano that was active in two stages. Three large central depression dissect the island, and large submarine debris-avalanche deposits are found offshore. The latest eruptions of Piton des Nieges occurred as recently as about 12,000 years ago.

Mauritius
The island of Mauritius, located along the Reunion hot spot track NE of Reunion Island, is a massive shield volcano that was active from 7.8 million years to about 30,000 years ago.

Rodriguez Island
Rodriguez Island lies along the Rodriguez Fracture Zone about 650 km east of Mauritius Island. The 18 x 6.5 km wide island is consists of a basaltic shield volcano of probably Plio-Pleistocene age. K-Ar ages of 1.54 and 1.32 million years were obtained from lava flows (Upton et al., 1967).

Hautere
New Zealand
Hautere (Solander Island) is an eroded volcano lying 40 km south of the tip of South Island, NW of Steward Island. Argon/Argon dates as young as about 400-150 ka were obtained by Mortimer et al. (2008).

Kaimai
New Zealand
The Kaimai area contains eight major outcrops of Pliocene and lower Pleistocene rhyolites (Skinner 1986). Houghton (1994 pers. comm.) found no evidence for Pleistocene domes at Kaimai.

Karioi
New Zealand
The eroded Pliocene to lower Pleistocene Karioi stratovolcano lies along the Tasman Sea and is the westernmost volcano of the Alexandra volcanic group. Potassium-Argon (K-Ar) dates for Karioi itself range from 2.92-2.16 million years ago (Ma), but scoria cones, tuff rings and basaltic lava flows primarily on the northern and eastern flanks are in part younger than the youngest K-Ar date of 1.8 Ma (Briggs 1983).

Pirongia
Latitude: 38°S
Pirongia is low-angle eroded stratovolcano of Pliocene-lower Pleistocene age of the Alexandra volcanic group. Potassium-Argon dates of 2.25 and 2.06 million years ago have been obtained from Pirongia, but flank cones are younger (Briggs 1983).

Kakepuku
Lava cone(s)
Kakepuku is less eroded than neighboring Pliocene-lower Pleistocene Pirongia volcano (Briggs 1983). A flank cone lies to the north, and the Te Kawa lava cone, the only volcano of the Alexandra volcanic group to retain a crater, lies to the SE.

Kaitake
Kaitake, an eroded, heavily vegetated Pleistocene volcano, is the NW-most stratovolcano of the Taranaki volcanic region.

Pouakai
Pouakai volcano, NW of Egmont, is an eroded Pleistocene stratovolcano surrounded by a ring plain of lahar deposits dating from about 0.25 million years ago (Neall et al. 1986). The relationship of German Hill cone, 10 km to the NE, to Pouakai is not clear.

South Auckland
Shield(s)
The South Auckland (Pukekohe) volcanic field consists of basaltic shield volcanoes, scoria cones and tuff cones and rings from 1.56-0.51 million years ago (Smith, in Johnson et al. 1989). The Ngatutura scoria cone group across the Waikato River is of late Plioceneto early Pleistocene age.

Mokohinau Islands
The Mokohinau Islands are the surface expression of a largely submarine rhyolitic plateau and are a part of the Hauraki volcanic region offshore from the Northland Peninsula. Burgess Island contains rocks of basaltic to rhyolitic composition. FanalIsland consists of a rhyolitic lava dome with an obsidian cap that is fission-track dated at 0.5 million years ago (Skinner 1986). Houghton (1994 pers. comm.) considers this date to be suspect.

Little Barrier
Little Barrier Island, part of the Hauraki volcanic region, is a Pliocene to Pleistocene dacitic to rhyodacitic stratovolcano, with its latest stage of activity taking place from 1.6-1.2 million years ago (Lindsay et al., 1999).

Mercury Islands
The Mercury Islands, thought to be Pleistocene in age on the basis of degree of preservation of scoria cones and relationship to terraces, are at least in part Miocene to Pliocene (Skinner 1986). The islands contain rhyolites and basalts.

Alderman Islands
The Alderman Islands are part of the eroded lava domes of the Minden Rhyolites, part of the Miocene to Pleistocene Whitianga Group (Skinner 1986) and are considered to be Pliocene or lower Pleistocene in age (Latter 1985, pers. comm.).

South Coromandel Peninsula
The southern Coromandel Peninsula contains three areas where Pleistocene basalts outcrop--Table Mountain west of Tairua Harbour, an area NW of Whangamata and a larger area between Te Aroha and Athenree (Latter 1985, pers. comm.). Houghton (1994 pers. comm.) notes that age data for many of the Coromandel localities is suspect, and that it is possible that all of the Coromandel arc volcanoes are Miocene-Pliocene in age.

Solander Island
The 1.5-km-wide Solander Island is the emergent surface of an isolated Pleistocene andesitic stratovolcano off the southern end of South Island. A Potassium-Argon date of about 1 million years ago was obtained by C J D Adams (Reay 1986).

Moutohora Island
Complex
Moutohora (Whale) Island forms the summit of a largely submerged Pleistocene dacitic-andesitic complex volcano that lies 11 km offshore from Whakatane in the Bay of Plenty. The island is 15 x 5 km wide and elongated E-W. The 354-m-high central dome complex is flanked by East Dome, which forms the eastern tip of the island and is the oldest of the domes, and Pa Hill lava dome, which forms the NW tip of the island. Acid hot springs, steaming ground, and fumaroles are located primarily between the central cone and East Dome. The central cone and east dome are both older than the roughly 42,000 before present (BP) Rotoehu Tephra, and Pa Hill dome is overlain by the 9000 years BP Rotoma Ash but may be considerably older. It was included in the Catalog of Active Volcanoes of the World (Nairn and Cole, 1975) based on its thermal activity.

Rotorua
The 22-km-wide Rotorua caldera is the NW-most caldera of the Taupo volcanic zone. It is the only single-event caldera in the Taupo Volcanic Zone and was formed about 220,000 years ago following eruption of the more than 340 km3 rhyolitic Mamaku Ignimbrite. Although caldera collapse occurred in a single event, the process was complex and involved multiple collapse blocks. The major city of Rotorua lies at the south end of the lake that fills much of the caldera. Post-collapse eruptive activity, which ceased during the Pleistocene, was restricted to lava dome extrusion without major explosive activity. The youngest activity consisted of the eruption of three lava domes less than 25,000 years ago. The major thermal areas of Takeke, Tikitere, Lake Rotokawa, and Rotorua-Whakarewarewa are located within the caldera or outside its rim, and the city of Rotorua lies within and adjacent to active geothermal fields.

Rungapapa Knoll
Submarine
Rungapapa Knoll, a seamount in the Bay of Plenty 17 km WSW of White Island, has an internal heat source (Latter 1985, pers. comm.). No eruptions are known.

Kapenga
Caldera(s)
The Kapenga volcanic center was active from sometime between 890 to 710 thousand years ago (ka) and again from about 280 to 270 ka and contains two collapse structures and rhyolitic lava domes (Wilson et al. 1984, Houghton et al. 1995). The NE center, previously considered part of the Okataina center, contains numerous pre-50 ka rhyolitic domes and was the source of the ca. 65 ka Earthquake Flat Breccia. No eruptive activity is known from the Holocene.

Mangakino
The Pleistocene Mangakino volcanic center has been the source of large-volume rhyolite ignimbrites erupted between 1.6 and 0.9 million years ago (Ma) (Wilson et al., 1984; Houghton et al., 1995). Two principal periods of activity occurred, from 1.6 to 1.53 Ma and 1.21 to 0.9 Ma (Wilson et al., 1995a). One of the largest ignimbrite eruptions of the Taupo volcanic zone took place at 1.21 Ma from Mangakino. The Titiraupenga and Pureora andesitic lava domes lie just to the south of the inferred caldera margin.

Northern Tongariro Group
A group of Pleistocene andesitic stratovolcanoes lies between Lakes Rotoaira and Taupo and to the west, forming the northern end of the Tongariro volcanic center. The Rotopounamu graben, trending SW from Lake Taupo, cuts Pihanga volcano, and is these of several young cones and craters less than 20,000 years old (Cole et al. 1986).

Rumble I
Submarine
Summit Elev: -1100 m

Antipodes Island
The isolated, uninhabited Antipodes Islands are located in the south Pacific, 770 km SE of New Zealand. Volcanism has been dominantly pyroclastic, and the presence of well-preserved scoria cones suggests a Holocene age (LeMasurier and Thomson, 1990). The most recent eruptions occurred on the cone forming Mount Galloway and Mount Waterhouse at the center of 4-km-wide main island. Marine erosion has exposed sections through tuff cones at Perpendicular Head and Albatross Point at the NE and SE tips of the island, respectively. Radiometric dates indicated basalts that are younger than 1 million years (250-500 ka with high uncertainty W of Reef Point), and Cullen (1969) also speculated that volcanism may have begun in the Tertiary and persisted "almost to the present day."

Rumble II East
Summit Elev: -1150 m
Subfeature of Rumble II

Thompson
Summit Elev: -1250 m

Silent II West

Silent II East

Yokosuka

Rapuhia

Giljanes

Kibblewhite

Sonne

Ngatoroirangi

Kuiwai

Haungaroa

Oliver-Speight

Cole

Hinetapeka
Kermadec Islands

Volcano OP
Kermadec Islands

Putoto
Kermadec Islands
Seamount in the northern Kermadec islands, about 160 km N of Raoul Island.

Volcano Q

Gamble

Rakahore

Hinepuia

Ata Volcanic Complex
Tonga Islands

Toku
Tonga Islands
The island of Toku, about 20 km SE of Fonualei, is the emergent summit of a large submarine volcano. No eruptions have been recorded, but it is at the north end of the active Tofua Arc, making at least Pleistocene activity likely.

Tonga Islands
Bathymetry appears to show a large cone-like structure with a 5-km-diameter caldera located midway between Metis Shoal (25 km NNE) and Kao (25 km SSW). Although no reports of volcanism are known from this feature, it is directly along the active Tofua volcanic arc, and has likely erupted within the Pleistocene.

Feinga Seamount
The bathymetry of this seamount shows a 4-km-diameter caldera open to the N, in which a dome appears to have grown. The edifice is located along the trend of the Tofua volcanic arc, about 43 km SSW of Tofua and 32 km NE of Fonuafo'ou (Falcon Island). Although no reports of volcanism are known from this location, it has likely erupted within the Pleistocene.

Rose Island
Samoan and Wallis Islands
The easternmost volcanic pile of the Samoa Islands, Rose Island is a coral atoll with sand beaches constructed on a volcanic basement in late-Pleistocene time (Stearns, 1944).

Nairai
Fiji Islands
Complex
Nairai is composed of five basaltic volcanic centers of Pliocene age; the well-preserved Pleistocene cinder cone Rairainiika is located on the NW coast.

Waikama
Fiji Islands
Complex
Waikama volcano comprises much of the northern end of Ngau Island and appears to have been active well into the Pleistocene (Coulson 1976).

Mago
Fiji Islands
A K-Ar date of about 0.3 million years was obtained from a basaltic rock from Mago Island on the Lau Ridge (Cole et al., 1990). Three scoria cones and short lava flows, some of which contain peridotite xenoliths, are located on the island.

Katafaga
Basaltic rocks from Katafaga Island on the Lau Ridge were K-Ar dated at about 1.6 million years (Cole et al., 1990).

Kabara
Basaltic rocks from Kabara Island on the Lau Ridge were K-Ar dated at about 1.0 million years (Cole et al., 1990).

Vokeo
Northeast of New Guinea
The westernmost volcano of the Quaternary Bismarck volcanic arc, Vokeo is a dissected, forest-covered volcano with a central basin. It is the only Bismarck arc volcano surrounded by a raised coral reef. Two thermal areas are present on the north coast (Johnson et al. 1972).

Viai
Northeast of New Guinea
The 4.5-km-long arcuate island of Viai (or Wei) is a remnant of a larger volcano. One thermal area is present on the N coast (Johnson et al. 1972).

Crown Island
Northeast of New Guinea
The deeply dissected 3-km-wide Crown Island is covered by rain forest. There is no known thermal activity or recorded eruptions. Young tephras on the island probably originate from Long Island (Johnson et al., 1972). Possible submarine debris-avalanche deposits lie both north and south of the island (Silver et al., 2009).

Bagabag
The 7 x 8 km Bagabag island is truncated by a 3 x 5 km crater that is breached by the sea on the SE side. A shallow ridge marks the submerged portion of the crater rim. An offshore reef rings the island (Johnson et al. 1972).

Tolokiwa
The circular 8-km-wide island of Tolokiwa contains a summit crater breached to the NE that is largely filled by a later cone. The volcano is of Quaternary age (Johnson et al. 1972). The largest documented submarine debris-avalanche deposit mapped in the Bismarck Arc lies north of Tolokiwa (Silver et al., 2009).

Tangi
New Britain
The dissected Tangi stratovolcano, occupying the southern end of New Britain's Cape Gloucester Peninsula, contains a breached summit crater and a single flank cone on the SW flank. The degree of erosional dissection suggests activity ceased during the Pleistocene (Johnson et al. 1971).

Unea
New Britain
A 6-km-wide caldera rim forms the margin of Unea Island, which contains three post-caldera domes. The volcano is largely of Pleistocene age, although Holocene activity cannot be ruled out (Johnson 1990, pers. comm.).

Narage
New Britain
The small forested island of Narage is the northernmost of the Witu (or Vitu) Islands, which lie north of western New Britain. Narage is the summit of a Pleistocene stratovolcano that displays strong thermal activity, and was included in the Catalog of Active Volcanoes of the World (Fisher, 1957) based on its geothermal activity. Boiling springs and a geyser are found along the SE and SW coasts; in 1863 a geyser 45 m high was observed at a sandbank 8 km offshore. A fringing reef, prominent on satellite imagery, encircles the island at a distance of 200 m to 400 m and encloses a narrow lagoon.

Lotomgan Group
A group of small Quaternary andesitic and rhyolitic volcanoes are located south of Bola volcano (Lowder and Carmichael 1970).

Bangum
Bangum is a Pleistocene stratovolcano dissected to much the same stage as the Garbuna volcanoes (Johnson and Blake 1972; Johnson 1990, pers. comm.). IAVCEI lists a thermal area, but gives a coordinate that appears to be at the west foot of Welcker volcano. Johnson and Blake note no thermal areas on Bangum.

Oto Group
The Oto volcanic group consists of five stratovolcanoes and a caldera of early to late Pleistocene age. The oldest volcanoes, Ko and Husa, are about 800-900,000 years old, and the steep-sided Oto, Mululus and Mateleloch volcanoes range from about 190,000 to less that 70,000 years old (Blake and McDougall 1973, Johnson and Blake 1972). The 4-km-wide Busui caldera of probable Pleistocene age is formed in a broad, low-angle cone of dominantly pyroclastic material. The names of Oto, Mululus and Mateloch peaks on published maps differ from that used by local inhabitants and in the geological literature.

Likuruanga
Likuruanga is a dissected, low stratovolcano with a large crater breached to the north. In September 2006, a boy died of carbon dioxide asphyxiation in a hole at Bakada village on the volcano's N flank.

Doma Peaks
New Guinea and D'Entrecasteaux Islands
The Doma Peaks, at the western end of a volcanic chain in the highlands of Papua New Guinea, are dominated by two westward-facing escarpments of probable landslide origin. Satellite cones and lava domes occur on the NE and S flanks of the dominantly andesitic volcano. There is no evidence for magmatic eruptions within the last few hundred or possibly few thousand years (Mackenzie and Johnson, 1984). A reported eruption within the past few hundred years was actually from Long Island, and an older lahar mentioned by Blong (1979) was not accompanied by any significant tephra production (Blong, 1982).

Crater Mountain
New Guinea and D'Entrecasteaux Islands
Crater Mountain, an arcuate chain of peaks, is extensively eroded to the point that its volcanic origin is almost unrecognizable. However, steep-sided valleys to the N and E are floored by lava flows and other young volcanic features. The easternmost Agotu Valley contains several small craters, cinder cones, and maars of late-Pleistocene or Holocene age (Mackenzie and Johnson, 1984). Several small cones, lava domes, and associated lava flows N and NW of the Erun Anticline may, in part, be Holocene in age.

Yelia
New Guinea and D'Entrecasteaux Islands
Mount Yelia, first recognized as a volcano in 1963, contains a group of andesitic lava domes in the summit area and NW flank. Marble Peak is an older volcanic center immediately to the south. The largest dome in the summit crater is perforated by at least 11 craters. Two large steep-sided, flat-topped lava domes occupy the NNE flank, and two smaller domes are located to the west. The last significant eruption occurred about 18,000 years ago, and no direct evidence for Holocene eruptions has been observed. Weak solfataric activity is present and there was an unverified report from local inhabitants of an eruption during the early 1940's. Weak fumarolic activity continues in the summit crater.

Kerewa
Mt. Kerewa is a deeply dissected Pleistocene andesitic stratovolcano south of Doma Peaks. A group of small cones, craters and domes is located to the west, and Mt. Ne is situated immediately to the NE (Mackenzie and Johnson 1984).

Sisa
Mt. Sisa is a deeply dissected Pleistocene stratovolcano with a large U-shaped depression open to the SW that may have originated by slope failure (Johnson 1987).

Bosavi
Mt. Bosavi is a truncated Pleistocene basaltic to andesitic stratovolcano with a 5-km-wide erosion caldera enlarged by the Turama River through a narrow breach on the SE. A group of cones, craters and maars are scattered over the plains to the SW of Bosavi (Mackenzie and Johnson, 1984).

Darai Hills
A group of Pleistocene cones and craters are scattered over a limestone karst plateau SE of Mt. Bosavi (Mackenzie and Johnson 1984).

Biwau Hills
The Pleistocene Mt. Biwau consists of two coalescing cones surrounded by lavas and probable lahar deposits. The northern cone is capped by a spine-like peak and a dome-like protuberance 1.5 km to the east. A small cinder cone lies 17 km to the west (Mackenzie and Johnson 1984).

Sugarloaf
The Pleistocene Sugarloaf Volcanic Field is composed of a group of coalescing lava domes, with several small cinder cones, explosion craters and maars (Mackenzie and Johnson 1984).

Hagen
Mt. Hagen is comprised of three coalescing stratovolcanoes with NW-facing escarpments that may result from slope failure (Johnson 1987). Potassium-Argon dates of 0.42 and 0.22 million years ago have been obtained (Mackenzie and Johnson 1984).

Giluwe
Mt. Giluwe is the only Papua New Guinea Highlands shield volcano and the highest Quaternary volcano of Papua New Guinea. The 30-km-wide basaltic-andesitic volcano is dotted with numerous parasitic cinder cones and lava domes; the upper slopes are heavily dissected by glaciers. The latest volcanism may post-date the younger glaciation that lasted until about 23,000 before present (Blake of Loffler 1971).

Ialibu
The Pleistocene Ialibu stratovolcano is morphologically complex, with deeply eroded gorges and a major fault zone that cuts the entire edifice. In contrast to many other Highlands volcanoes, the most mafic basaltic rocks are topographically higher than andesitic rocks (Mackenzie and Johnson 1984).

Murray
The Pleistocene Mt. Murray stratovolcano straddles WNW-trending limestone ridges and contains a large 6-km-wide crater breached to the south that may have originated from slope failure (Johnson 1987). Two parasitic cones are situated on the NE and SE flanks.

Suaru
Suaru is a conical Pleistocene stratovolcano with three satellitic cones on the east flank. The volcano is extensively modified by seven narrow valleys that radiate from the dissected summit region (Mackenzie and Johnson 1984).

Karimui
The Pleistocene Karimui volcano is composed of 3-5 closely spaced eruptive centers extensively modified by a complex 17-20 km wide erosion caldera (Mackenzie and Johnson, 1984).

Duau
The Pleistocene Mt. Duau is dominated by a 10-km-wide breached escarpment that may result from slope failure (Johnson, 1987). A slide block that includes the summit crater is located at the head of the escarpment.

Favenc
The Pleistocene Mt. Favenc has a SW-facing escarpment similar to that of neighboring Duau that may originate from slope failure, although the structural relationships are less clear than on Duau (Johnson, 1987).

Aird Hills
The Aird Hills are a group of Pleistocene andesitic and dacitic lava domes that rise above the Kikori River delta (Mackenzie and Johnson 1984).

Trafalgar
Mount Trafalgar is a deeply dissected stratovolcano of Pleistocene age (Smith and Davies, 1976).

Tabar
New Ireland
Tabar Island, the southernmost of the Tabar island group, consists of two partially coalescing Pleistocene volcanoes connected by a low isthmus. The younger, southern cone contains a 3-5 km wide depression breached to the SE.

Tanga
New Ireland
Malendok, Lif and Tefa islands are remnants of the summit of a mostly submerged stratovolcano. In the center of the caldera, the small islands of Bitlik and Bitbok mark remnants of early Pleistocene post-caldera lava domes marking the volcano's latest activity. A small hot spring on Malendok Islands marks the only current thermal activity.

Emperor Range
Bougainville and Solomon Islands
Caldera(s)
The Emperor Range in northern Bougainville Island is a group of strongly eroded volcanic centers of Pleistocene age. A poorly preserved caldera 5-6 km in diameter is filled by a lava dome complex. The Kunua complex immediately to the west contains a 3.5 x 4.5 km caldera that produced ignimbrites dated about 0.2 million years ago that reached the western coast.

Numa Numa
Bougainville and Solomon Islands
The broad, densely forested Numa Numa stratovolcano contains an erosion caldera more than 3 km wide with a lava dome immediately to the south. Extensive erosion suggests a Pleistocene age (Blake and Miezitis (1967).

Bakanovi
Bougainville and Solomon Islands
Bakanovi is the deeply eroded crescentic remnant of an andesitic stratovolcano about 15 km east of Bagana volcano. Its poor state of preservation suggests a Pleistocene or even Pliocene age (Blake and Miezitis, 1967).

Nonda
Nonda volcano, the youngest volcanic feature of Vella Lavella Island, is a lava dome located within a well-preserved crater. No historical eruptions have been reported, although inhabitants reported "smoke" and explosive activity in the vicinity of andesitic Nonda Hill at the time of a major earthquake in 1959 (Taylor, 1976). Vella Lavella Island was mapped as several coalescing Pliocene to possibly Pleistocene volcanic centers (Solomon Islands Geological Survey, 1982). Nonda was included in the Catalog of Active Volcanoes of the World (Fisher, 1957) based on its geothermal activity. The Paraso thermal area displays solfataras, hot springs, and boiling mud pots.

Maetambe
The degree of erosion suffered by the latest ash flows suggested activity within the last few hundred years at the most (Coleman 1960). Later mapping indicates an older age--Pliocene to possibly Pleistocene (Ridgway and Coulson 1987).

Kolombangara
Kolombangara is a Pleistocene stratovolcano with young scoria cones on the western and NE flanks. No Holocene rocks have been mapped (Solomon Is Geol Surv, 1982). Thermal areas are also present (Grover, 1955).

Rendova
Rendova Island consists of a Pliocene to Pleistocene basaltic volcano on the north and uplifted submarine lavas to the south.

Mbareke
The Pliocene to Pleistocene Mbareke volcanic center consists of a core of basaltic andesite to andesite lavas and breccias overlain by a thick pile of olivine basalt lavas. An andesitic plug lies on the southern rim of the dissected summit crater.

Vangunu
Longitude: 158°E
The Pliocene to Pleistocene Vangunu volcano has two deeply eroded central craters breached on their southern sides.

Nggatokae
Nggatokae consists of a well-formed volcanic cone of Pliocene to Pleistocene age with a breached central crater and a subsidiary scoria cone on the northern flank<.

Ureparapara
Vanuatu
The 8-km-wide Ureparapara Island is topped by a 5-km-wide erosional caldera that is breached by the sea on the NE. Sapper (1917) states that Ureparapara must have still been active in 1872, but the the latest activity occurred during the Pleistocene (Ash et al. 1980).

Mota
Vanuatu
The 5-km-wide Mota Island is comprised of the eroded vent-filling intrusive of a Pleistocene volcano that rises above a wide raised Holocene platform of reef limestones.

Merig
Vanuatu
A andesite plug dated 1.1 million years ago surrounded by basaltic and andesitic breccia is all that remains above sea level on the tiny island of Merig (Macfarlane et al. 1988).

Paama Island
Williams & Warden (1964) report an eruption of Paama in 1897 (p 54) but Warden (1967) reports extensive erosion has destroyed the original volcanoes on Paama and classifies them as older than the Pliocene-early Pleistocene volcanoes of Emae.

Emae
Williams and Warden (1964) report historical activity on Emae and some ashfall, which could have originated from another island (Eissen et al. 1991). Warden (1967) reported destruction of summit craters by erosion and deep dissection of surficial deposits, and suggests the Emae volcanoes may have become extinct in the Pliocene or early Pleistocene. Crawford et al. (1988) place Emae on the rim of a large caldera that extends south to Mataso Island. Macfarlane et al. (1988) place two smaller uncertain calderas at this location. Eissen et al. (1991) did not find evidence for a caldera at this location.

A submarine volcano with a central crater was discovered during a 1984 survey along the active volcanic arc SE of Emae Island and NE of Efate Island (Crawford et al. 1988).

Fatmalapa
Largely submarine basaltic eruptions during the Pleistocene from 1.5 to 0.9 million years ago constructed composite volcanoes on northern Efate Island (Macfarlane et al. 1988).

William
The low basaltic William stratovolcano of Pleistocene age dominates the northern end of Erromango Island. Headward erosion by streams has excavated a 5-6 km diameter erosion caldera which is partially filled by a basaltic lava plug (Colley and Ash, 1971).

Pumpan
The eroded Pleistocene basaltic Pumpan volcano occupies the center of Erromango Island. Rocks are dominantly pyroclastics overlain by widespread thick lava flows (Colley and Ash, 1971).

Melkum
The eroded Pleistocene Mt. Melkum stratovolcano occupies the west-central part of Erromango Island, along with several other small stratovolcanoes.

East Tanna Volcano
Volcanic rocks forming much of the northern part of Tanna island originated from the Pleistocene East Tanna Volcano, now largely collapsed below sea level on the eastern side of the island (Robin et al. 1993). Lavas and pyroclastics along the east coast of the island have a westward dip. The Green Hill volcanics at the northern end of the island (Carney and Macfarlane 1979) can be considered a subordinate center to the East Tanna Volcano.

Maer Volcanic Province
Australia
Eight small islands in the NE part of the Torres Straits form the northernmost east-Australian Cenozoic volcanic field. The Quaternary pyroclastic cones have been dated between 3 and 1 million years ago (Stephenson, in Johnson et al. 1989).

Piebald Volcanic Province
Australia
Shield(s)
The Piebald volcanic province consists of eroded small shield volcanoes and pyroclastic cones dated between 1.6 and 1.2 million years ago (Stephenson, in Johnson et al. 1989).

Mclean Volcanic Province
Australia
The McLean volcanic province consists of Tertiary volcanoes and undated younger scoria cones and valley-floor lava fields that are probably less than 1 million years ago (Stephenson, in Johnson et al. 1989).

Atherton Volcanic Province
Shield(s)
The Atherton volcanic province covers an area of 1800 km2 and contains 52 eruptive centers, including small lava shields, cinder cones, maars, and one diatreme. The maars, the only ones in Northern Queensland, range in age from 200,000 to 10,000 years before present (Stephenson, in Johnson et al. 1989).

McBride Volcanic Province
An area of around 5500 km2 is covered by the broad lava plains and cones of the McBride volcanic province. The 164 volcanic centers form a broad topographic dome. One lava flow traveled 160 km from Undara crater. The youngest volcano is dated 70,000-50,000 BP (Stephenson, in Johnson et al. 1989).

Fox
Mount Fox is a pyroclastic cone distinct from the large volcanic provinces of NE Australia. Young basanite lava flows dated 1.5 million years ago descend the coastal scarp into the Stone River valley (Stephenson, in Johnson et al., 1989).

Chudleigh Volcanic Province
Straddling the Great Divide, the Chudleigh volcanic province contains 46 vents and covers an area of 2000 km2. Several lava shields and numerous pyroclastic cones are present; the youngest dated rocks are 0.25 Ma. Two lava flows traveled 100 km from their source (Stephenson, in Johnson et al. 1989).

Nulla Volcanic Province
The Nulla volcanic province consists of 46 vents and associated lava flows covering an area of 7500 km2. The youngest volcano, Toomba, is only 13,000 years old, and produced a massive 120 km long lava flow. Three other lava flows exceed 100 km length (Stephenson and Griffin 1976).

Sturgeon Volcanic Province
Wide lava plains of the Sturgeon volcanic field cover 7500 km2. The youngest lava flow is dated at 0.92 Ma and traveled 120 km from its source at Twins crater (Stephenson, in Johnson et al. 1989).

Bundaberg-Boyne Province
The Hummmock (1.1-0.9 million years ago) (Ma), Berrembea, and Barambah (0.6 Ma) basalts from the Bundaberg, Gin Gin and Gayndah areas, respectively, are of Pleistocene age. The northern Boyne area has also had Pleistocene volcanism (Robertson, Sutherland and Hollis, inJohnson et al. 1989).

Imun
Sumatra
Lava cone
Imun is a single small dacitic and/or rhyolitic cone south of Lake Toba with a youthful, undissected morphology. It is surrounded by and sits over Toba tuffs, and is considered to be of late-Pleistocene/Holocene age (Aldiss et al., 1983; Ryberg et al., 2016). Nukman and Moeck (2013, reproduced in Niasari, 2015) mapped it as Pleistocene. Imun lies along the Sumatra Fault, and magmatic processes in this region appear to be related to activity on this fault (Muksin et al., 2013).

Kunyit
Sumatra
Kunyit volcano lies about 10 km S of Lake Kerinci, well to the N of its location listed in Neumann van Padang (1951). The summit of the dacitic volcano contains two craters open to the S, the uppermost of which has a small crater lake. The age of the latest eruptive activity is not known, but there do not appear to be any recent volcanic features. Fumarolic activity occurs at the youngest crater on the N side of the summit area. Social media reports from hikers confirmed hot springs and sulfur odors along the trail in 2013. Silitonga et al. (2015) mapped the most recent volcanic unit as late Pleistocene while researching the area as a geothermal energy prospect.

Besar
Sumatra
Stratovolcano?
The Gunung Besar stratovolcano in SE Sumatra was characterized by Neumann van Padang (1951) as a solfatara field (Marga Bajur (or Bayur) on the NW and N foot of the edifice. The crater was noted as having an "unimportant" sulfur deposit in its crater and vapor exhalation. The remaining edifice of Besar consists of about 50% of a crater rim completely open to the E, with three small domes or cones, the largest of which contains a small pond in a summit crater. The geothermal area was described by Neumann van Padang (1951) as including four small solfatara fields: Gemurah Badas (8 x 10 m with hot springs and sulfur gas exhalation), Gemurah Bubur (large basin of boiling water formed between 1930-40), Gemurah Keningan (boiling mud springs, very active 1938-40), and Gemurah Ilahan (2 km upstream of Badas with geyser-like mud springs and dead trees). A "phreatic steam eruption" in April 1940 was noted from Gemurah Ilahan. Hochstein and Sudarman (1993) considered the Marga Bayur geothermal system to be "associated with a degassing magma chamber because radiometric dating of the youngest tuff deposiuts (unpublished data, Pertamina files) showed that [the volcano had been] active during the last 30 kyr." This geothermal prospect has been studied but not yet developed.

Pulau Weh
Pulau Weh island off the NW tip of Sumatra has been interpreted as the remains of a partially collapsed older center breached to the NW and filled by the sea. Pulau Weh was included in the Catalog of Active Volcanoes of the World (Neumann van Padang 1951) based on its geothermal activity. Volcanism was assumed to be of Pleistocene age (Bennett et al., 1981), but fumaroles and hot springs are found a NW-E-trending line along the summit of the island and near the western shore of Lhok Perialakot bay on the northern side of the island.

Seulawah Inong
Seulawah Inong is mapped as a Quaternary volcano (Bennett et al. 1981).

Olim
Fissure vent(s)
The Olim volcanics are Pleistocene porphyritic andesitic volcaniclastics erupted from fissure vents (Bennett et al., 1981, Keats et al., 1981).

Teu Minas
Teu Minas is a small eroded Pleistocene andesitic stratovolcano with local thin basalt lava flows (Keats et al. 1981). Porphyritic andesite is also present at the volcanic center (Rock et al., 1982).

Geureugoh
Fissure vent(s)
The Geureugoh volcanics are mapped as andesitic pyroclastic breccias originating from fissure vents (Keats et al. 1981).

Meugeurinceng
Fissure vent(s)
The Meugeurinceng volcanics are mapped as andesites of Pleistocene age, possibly fissure fed (Cameron et al. 1983).

Gunung Tudeuk
Gunung Tudeuk is a recently extinct Pleistocene andesitic to dacitic lava dome (Keats et al. 1981, Cameron et al. 1983).

Nama Salah
Nama Salah is mapped as pumiceous andesites and dacites of Pleistocene age (Cameron et al. 1983). Lahars from Nama Salah blocked drainages, forming lake Laut Tawar.

Gunung Telago
Gunung Telago is mapped as a complex double volcanic center of Pleistocene age (in part Pliocene) by Cameron et al. (1983).

Gunung Sembuang
Explosion crater
Gunung Sembuang is an andesitic Pleistocene explosion crater with a lava flow (Cameron et al. 1983).

Geureudong
Geureudong is a massive, 30-km-wide complex that rises above schists and granitic rocks and is one of the largest volcanic complexes in NW Sumatra. The 2885-m-high Bur ni Geureudong is Pleistocene in age, but hot springs are found on its northern and southern flanks. The Pupandji pyroclastic cone was constructed on its SE flank, adjacent to two maars with diameters of 300 and 60 m.

Kembar
The Gayolesten fumarole field is located on the flanks of the Pleistocene Gunung Kembar volcano. The Kembar complex, located at the junction of two fault systems, is an andesitic shield volcano capped by a complex of craters and cones (Cameron et al. 1982). Gayolesten was included in the Catalog of Active Volcanoes of the World (Neumann van Padang 1951) based on its geothermal activity. Active fumaroles and hot springs are present at several locations.

Bekulap
Lava dome(s) ?
The Bekulap volcanic center consists of three possible lava domes and an explosion crater of Pleistocene age (Cameron et al. 1982). The Palpalan and Sumilir volcanoes of IAVCEI (1973) near this location are mapped (Paipalan and Semilir) as sedimentary rocks by Cameron et al. (1982).

Takur-Takur
Takur-Takur (Takor) is a dissected volcano composed of plagioclase-hornblende-phyric dacite and mapped as Pliocene to Pleistocene in age (Rock et al., 1983; Cameron et al. 1982).

Bukit Tenaroh
Bukit Tenaroh is mapped as Pliocene to Pleistocene (Cameron et al. 1982).

Simbolon
Simbolon is a Pleistocene volcano with a large summit caldera and several flank lava plugs (Cameron et al. 1982).

Martimbang
Martimbang is an andesitic volcano of Pleistocene age (Aspden et al. 1982).

Melintang
Melintang (also known as Malintang or Gunung Sago) is a andesitic to basaltic volcano of Quaternary age with a crater breached to the SE (Silotonga and Kastowo 1975).

Maninjau
Maninjau caldera is the largest silicic volcanic center in the Padang area of central Sumatra. The elongated caldera, filled by a lake, was formed during three Pleistocene eruptive episodes. K-Ar dating on the andesites and tuffs surrounding the caldera yielded ages of 0.83 +/- 0.42 Ma for older pre-caldera andesites (Barber et al., 2005). The youngest rhyolitic ashflow deposit was dated at about 0.28 +/- 0.12 million years (Leo et al., 1980; Barber et al., 2005).

Bukit Telor
Bukit Telor, also known as Bukit Ibul, is a basaltic cone located along the northern coast of Sumatra, more than 200 km behind the axis of Quaternary volcanism. It is only about 38 m high, but the total outcrop of the basalts is as much 4 km2 in area (Barber et al., 2005). The K-Ar age of these basalts is about 1.25 +/- 0.19 million years. As with Sukadana and because of its back-arc location, Bukit Telor basalts are quite texturally and compositionally different from the arc volcanics. Lherzolite mantle xenoliths are common, and the lavas typically range from quartz-tholeiite to mildly alkaline in composition (Barber et al., 2005).

Tujuh
Tujuh is a Quaternary volcano with a caldera partially filled by Lake Gunung Tujuh. A post-caldera composite cone, breached to the NW, fills the NW part of the caldera, giving the caldera lake a half-moon shape.

Runcing
Gunung Runcing was identified by Rosidi et al. (1976) as an early Quaternary volcano. The exact age is unknown, and it appears heavily eroded with about half of a remnant edifice rim on the west side.

Raja-Sabanda
Gunung Raja (or Raya) appears to be a remnant stratovolcano with a large caldera open towards the entire SE side that may originally have been about 3 km in diameter. The Bukit Sabanda cone lies about 2 km NE of the caldera. Although eroded, the volcanic features are still evident. Mapping related to geothermal exploration of the adjacent Kunyit volcano identified a "Raja volcanic unit" as Middle Pleistocene, but did not include this volcano in the mapped area that was published (Silitonga et al., 2015).

Hulunilo
The Hulunilo stratovolcano, about 5 km E of Sumbing volcano, has a caldera about 1.5 km in diameter that is breached to the W. Morphologically it appears no more eroded than other Quaternary edifices in central Sumatra, though the age of it's most recent eruption is unknown.

Tungkat
The small Bukit Tungkat about 10 km E of the Masurai complex exhibits an extensively eroded appearance, but is still a recognizable volcanic cone. Pleistocene activity is possible , although no ages are known.

Masurai
Gunung Masurai is a large volcanic complex with a remnant half-caldera and a chain of two summit crater lakes and a cone extending SW beyond the former caldera rim. Its youthful constructional phase suggests a late Pleistocene age (Sieh and Natawidjaja, 2000). The Masurai volcanic cluster is associated with the Sungai Penuh pull-apart basin, a feature of the Sumatra strike-slip fault, which becomes wider towards the volcanic cluster (Muraoka et al., 2010).

Isau-Isau
Isau-Isau is of Quaternary age, and though it was a predominantly andesitic volcano, it is part of the Pasoemah Highland ignimbrite complex (van Bemmelen 1949b; Westerveld, 1952). The edifice is mostly surrounded by andesites, dacites, and basalts from Isau-Isau and the surrounding stratovolcanos (Westerveld, 1952).

Bukit Nanti
Bukit Nanti is a young Quaternary volcano (van Bemmelen 1949b).

Raja
Raja volcano, located north of Ranau Lake, was mapped as a morphologically youthful volcano of likely late Pleistocene age (Sieh and Natawidjaja, 2000).

Pesagi
Pesagi volcano, a collapsed caldera located SE of Ranau Lake, was mapped as a morphologically youthful volcano of likely late Pleistocene age (Sieh and Natawidjaja, 2000; Widarto et al., 2016). However, Wahib (1998) suggests that Pesagi did erupt in the Holocene and that it is in part responsible for young volcanic breccias, tuffs, and andesites in the region. Despite its relative youth, the slopes are quite dissected in spots and approach angles as steep as 70 degrees near the summit (Wahib, 1998). These inherently unstable slopes collapsed in the wake of the 1993 Liwa earthquake, leading to destructive landslides.

Tanggamus
Gunung Tanggamus is of Quaternary age (van Bemmelen 1949b). Its products, which mostly consist of lavas, breccias, and tuffs of predominantly dacitic and andesitic composition, dominate the geology of the western part of the Lampung Province in southern Sumatra (Zulkarnain, 2011). Older Tanggamus products close to the main cone are generally pyroclastic breccias, consisting of porphyritic andesite and lapilli tuff. The younger products that make up the relatively undissected cone are of intermediate composition, and those deposits in the proximal zone surrounding the cone and in more distal regions are pyroclastic and laharic breccias and ignimbrites (Husein et al., 2015). The ignimbrites appear to be younger than the pyroclastic breccias (Husein et al., 2015). The lavas on Tanggamus are vesicular and porphyritic, and at about 1.4 million years old, are younger than the pyroclastic breccias and ignimbrites. The laharic breccias, consisting of porphyritic andesite and pumice, yielded an age of 1.5 Ma; however, field observations indicate that these units may be younger (Husein et al., 2015).

Sukadana Basalts
The low Sukadana Plateau, 30 x 11 km wide, is a volcanic expression of the Sukadana Basalts of Pleistocene age (Barber et al., 2005). The plateau itself covers an area of approximately 1000 km2 and contains fissure-fed lava flows 2-3 m thick issued from NW-SE trending fissures (Barber et al., 2005; van Bemmelen 1949b). The basaltic region may be over 200 m thick in areas, localized around eruptive centers, but no deposits greater than 10 m have been observed. Some columnar jointing is present. K-Ar dating gave ages ranging from 0.44 Ma to 1.15 Ma for the oldest samples (Soeria-Atmadja et al., 1985 in Barber et al., 2005), but more recent ages measured from more well-preserved flows and spatter cones are around 0.01 to 0.8 million years. Sukadana is technically part of the back-arc region of the Sumatra Volcanic Arc Segment, evidenced by notable textural and compositional differences from the arc volcanics, as well as a similarity to the back-arc Bukit Telor basalts (Barber et al., 2005).

Uruk Simacak
Converted from subfeature of Singkut caldera. Mapped as part of the Pliocene-Pleistocene QTvk unit (see Harahap, 2011; Aldiss et al., 1983; Cameron et al., 1982).

Barus
Converted from subfeature of Singkut caldera. Mapped as part of the late Pleistocene Qvbr unit of andesitic lavas and pyroclastics (see Harahap, 2011; Aldiss et al., 1983; Cameron et al., 1982).

Pesawaran-Ratai
Named for the two high points on the crater rim, the Pesawaran-Ratai edifice was probably a typical stratovolcanic cone that appears to have collapsed to the north, where the crater has breached. The volcano and surrounding area has been mapped as Quaternary on Indonesian geological maps (Mangga 1994, Suharno et al., 2015). Hot springs and geysers are present on the S flank (Suharno et al., 2015).

Bukit Lumut
Located in south-central Sumatra overlooking the Semalako Plain, Bukit Lumut has a 2.1-km-diameter crater open to the north. It was mapped by Budiardjo et al. (2001) as the Pleistocene 0.893 Ma Lumut Andesite. Two small hills within that unit, one of which is name Bukit Pabus, consist of the slightly older Pabus Tuff (0.895 Ma). The Hululais volcano and geothermal are lies immediately to the SE.

Bukit Tiga
Located in south-central Sumatra SSE of the Semalako Plain, Bukit Tiga has a 1.3-km-diameter crater open to the SW. It was mapped by Budiardjo et al. (2001) as the Pleistocene 0.984 Ma Tiga Andesite. The Hululais volcano and geothermal are lies immediately to the N.

Malabar
Java
The broad, forested, Gunung Malabar stratovolcano is located immediately south of the city of Bandung in western Java. While it was previously thought to be of possible Holocene age (Bronto 1995, pers. comm.), K-Ar dates of 0.23 Ma were reported by Bogie and Mackenzie (1997). Additionally, Malabar material was overlain by other Pleistocene deposits from the Wayang-Windu domes a few kilometers south. A geothermal energy project is present on the S flank closest to Wayang-Windu, but no active geothermal features have been reported.

Wayang-Windu
Java
Wayang-Windu, the site of a geothermal prospect, is a series of andesitic lava domes about 30 km S of Bandung and immediately S of Malabar volcano. Both Gunung Wayang and Gunung Windu have fumarolic areas. The age of the latest eruptive activity is not known, but Bogie and MacKenzie (1997) reported K-Ar dates of 0.49 Ma (G. Wayang), 0.19 Ma (G. Bedil), and 0.10 Ma (G. Windu).

Gunung Putri
Java
Gunung Putri is a peak in an area of eroded Quaternary volcanoes at the northern end of a chain extending north from Galunggung. The Kawah Karaha fumarole field about 1.4 km N of the summit covers an area of 250 x 80 m and contains a sulfur deposit. The Catalog of Active Volcanoes of the World (Neumann van Padang, 1951) reported an uncertain phreatic eruption in May 1861. Tripp et al. (2002) indicated based on drilling that the Kawah Karaha field is part of a geothermal system originating from an intrusive body below Telaga Bodas (Talagabodas).

Lurus
The small Lurus volcanic complex along the northern coast of eastern Java, north of the Iyang-Argapura massif, produced leucite-bearing rocks followed by later eruptions of andesitic and trachytic composition. This little known complex was mapped as subrecent-to-recent age by van Bemmelen (1949b). Ringgit, 30 km E also along the N coast of Java, was dated at 1.2-0.5 Ma.

Gede
Gede volcano on the NW tip of Java is of Quaternary age and is located about 280 km from the trench (van Bemmelen 1949b). The Gede Salak volcanic complex consists of pyroclastic flows on its western flanks and lava flows on its eastern flanks (Kurniawan et al., 2011). Mt. Gede is also surrounded by Plio-Quaternary tuffs (Banten Tuffs) ranging from 0.07 to 0.1 Ma in age (Pramumijoyo and Sebrier, 1991). Kurniawan et al. (2011) suggest that these Tuffs came from the calderas of the nearby Rawa Dano volcanic complex but gravity anomalies in the region suggest that neither Gede nor its nearby volcanoes could have been responsible for these ignimbrites and instead suggest a pre-existing caldera in the Sunda Straight was responsible (Nishimura et al., 1986).

Cibugis
Volcanoes in this portion of Java are Quaternary in age (van Bemmelen 1949b).

Kendeng
Kendeng is a stratovolcano of Pleistocene age characterized by andesites and andesitic breccias (Bronto, 1995, pers. comm.; Tun et al., 2014). These deposits cover older andesites and lapilli tuffs; unlike other volcanic deposits in western Java, they are not greatly affected by hydrothermal alteration (Tun et al., 2014).

Endut
Endut volcano ceased activity in the upper Pleistocene (van Bemmelen 1949b). The size of Gunung Endut suggests that it was a stratovolcano that underwent a summit crater breach and sector collapse, which may have been aided by hydrothermal processes (Bogie et al., 2010). Endut is a volcanic edifice that makes up a series of volcanoes framing the Gunung Salak Geothermal Field (Keetley et al., 2003). It is a largely andesitic volcano (Bogie et al., 2010).

Halimun
Activity at the NW-most of two adjacent volcanoes named Halimun ceased in the upper Pleistocene (van Bemmelen 1949b).

Halimun
Activity at the SE-most of two adjacent volcanoes named Halimun ceased in the upper Pleistocene (van Bemmelen 1949b). Halimun and Talaga are the two main peaks about 2.5 km apart along a ridge.

Sanggabuana
Volcanic activity at Sanggabuana, a stratovolcano in northwest Java, began in the late Tertiary, but continued into the Quaternary (Bronto 1995, pers. comm.; Soeria-Atmadja, 1998). K-Ar dating on a sample from an andesite lava outcrop yielded an age of about 5.35 Ma (Soeria-Atmadja et al., 1998). Products consist of lava flows alternating with pyroclastic and laharic breccias. There are also several andesitic plugs (Soeria-Atmadja et al., 1998). Sanggabuana is also associated with the Jatiluhur-Sanggabuana-Gunung Subang mineral belt (Soeria-Atmadja et al., 1998).

Kancana
Active in older Quaternary but extinct in Holocene (IAVCEI).

Tilu
Tilu volcano is of Pleistocene age (van Bemmelen 1949b).

Kancana
Kancana is a Quaternary stratovolcano (Bronto 1995, pers. comm.).

Mandalagiri
Volcanoes in this portion of Java are Quaternary in age (van Bemmelen 1949b).

Cikuray
Cikuray, a prominent stratovolcano SW of Garut, is of Quaternary age (van Bemmelen 1949b). Products mainly consist of lava flows of basaltic andesite, with some pyroclastic flow and lahar deposits (Abdurrachman and Yamamoto, 2012). Cikuray, along with Papandayan, are located within the Triangular Volcanic Complex of West Java, a group of Pliocene to Quaternary volcanoes (Abdurrachman et al., 2015; Abdurrachman and Yamamoto, 2012).

Kawah Kamojang
Kawah Kamojang, the first developed geothermal field in Indonesia, is located 7 km WNW of the historically active Guntur volcano within the Pleistocene Pangkalan caldera. Kawah Kamojang was included in the Catalog of Active Volcanoes of the World (Neumann van Padang 1951) based on its geothermal activity. The 1.2 by 0.7 km thermal area consists of fumaroles, steaming ground, hot lakes, mud pots, and hydrothermally altered ground. The field is located along a WSW-ENE-trending Quaternary volcanic chain that includes Gunung Rakutak, the Ciharus, Pangkalan, and Gandapura complexes, Gunung Masigit, and Gunung Guntur. This chain is progressively younger to the ENE. Kawah Kamojang is associated with the Pangkalan and Gandapura volcanic centers, along the Kendeng fault, which extends SW to the Darajat geothermal field.

Sedakeling
Sedakeling is a stratovolcano of Quaternary age (Bronto 1995, pers. comm.).

Mandalawangi-Haruman
Mandalawangi is stratovolcano of Quaternary age (Bronto 1995, pers. comm.).

Canlancang
Canlancang, at the NNE end of a group of volcanoes extending SSW to Papandayan, is of Quaternary age (van Bemmelen 1949b).

Cakrabuana
Cakrabuana is a Pleistocene stratovolcano (van Bemmelen 1949b).

Sawal
Sawal is a stratovolcano of Quaternary age (Katili and Sudradjat 1984a), with a large crater breached to the south.

Lasem
Lasem was active in middle upper Pleistocene (IAVCEI). Deposits have been dated to 1.6 - 1.1 Ma, and it appears to be the oldest and least potassic Quaternary volcano in the back-arc region of central Java (Leterrier et al., 1990). Lasem's products mostly consist of pyroclastic flow deposits, small lava flows, and dome extrusions. Composition is dominantly characterized by potassic calc-alkaline andesites, but there are also some basaltic andesites and dacites (Leterrier et al., 1990).

Selokaki
Selokaki is a Quaternary stratovolcano (Bronto 1995, pers. comm.).

Argowayang
Argowayang is a Quaternary stratovolcano (Bronto 1995, pers. comm.).

Ringgit
Ringgit volcano in eastern Java is of Plio-Pleistocene age, dated to about 1.2-0.5 Ma (van Bemmelen 1941; Leterrier et al., 1990). Eruptions mentioned by Von Wolff (1929) in 1586, 1593, and 1597 are attributed to Raung. Ringgit's products generally consist of leucite basanites and tephras (Leterrier et al., 1990).

Merbuk
Lesser Sunda Islands
Merbuk is mapped as a Quaternary volcano (Purbo-Hadiwidjojo 1971).

Patas
Lesser Sunda Islands
Patas is mapped as a Quaternary volcano (Purbo-Hadiwidjojo 1971).

Seraja
Lesser Sunda Islands
Seraja volcano at the eastern tip of Bali, is mapped as Quaternary (Purbo-Hadiwidjojo 1971).

Punikan
Punikan is a young volcanic cone, part of the Quaternary volcanic arc (van Bemmelen 1949b).

Ramu-Labumbu
This heavily eroded volcano has two peaks, Doro Ramu and Doro Labumbu, and is located abotu 30 km SE of Tambora. It was mapped by Garvin (2002, shown in Khant et al., 2013) as early Pleistocene.

Doro Lambuwu
Doro Lambuwu (or Lambuwa) is a broad Quaternary volcanic zone west of Bima Bay with a caldera open to the NE (Ratman and Yasin 1978). IAVCEI (1973) lists a Doro Oromboha volcano in this area. The area, about 30 km across, was mapped by Garvin (2002, shown in Khant et al., 2013) as early Pleistocene. The Garvin (2002) map also identified volcanic features named Doro Matua and Doro Pokah, but clearly identifying specific peaks in this heavily eroded region is difficult.

Doro Maria
Doro Maria is a large eroded stratovolcano at the NE end of Sumbawa Island of Quaternary age (Ratman and Yasin 1978). It was mapped by Garvin (2002, shown in Khant et al., 2013) as early Pleistocene, and includes the peaks named Doro Kuta and Doro Kota.

Doro Saboke
Doro Saboke, at the SE tip of Sumbawa Island, is a Quaternary volcano (Ratman and Yasin 1978). the area was mapped by Garvin (2002, shown in Khant et al., 2013) as Pliocene into early Pleistocene.

Gilibanta
Stratovolcano?
The small island of Gilibanta was reported by a pilot to be destroyed by a volcanic eruption in 1957, but the report has not been confirmed by scientific sources and is considered doubtful (Hantke 1962). Ratman and Yasin (1978) map Gilibanta Island as a Quaternary volcano with a caldera open to the north forming Ouingke Bay.

Doro Otota
Doro Otota at the southern end of Komodo Island, is a Quaternary volcano (Ratman and Yasin 1978).

Doro Ora
Doro Ora volcano forming the southern end of Rinja Island is of Quaternary age (Ratman and Yasin 1978). Nuso Kode within a bay at the southern end of the island is also of Quaternary age.

Gunung Beliling
Gunung Beliling is a Quaternary volcano (Ratman and Yasin 1978).

Ilikedeka
The Riang Kotang fumarole field is located at the northern foot of Quaternary Ilikedeka volcano near the eastern tip of Flores Island. Two fumarolic areas occur along the saddle on the northern foot of the volcano. Hot springs are located along the SW side of Oka Bay on the southern coast and Hadang Bay on the NW coast.

Sangenges
Sangenges (also known as Puncak Ngenges) was mapped as Pleistocene to early Holocene by Garvin (2002, shown in Khant et al., 2013). Edifices immediately NE (Sesset) and SE (Batu Lanteh) are interpreted as Miocene-Pliocene features. This volcanic group forms the northern part of western Sumbawa, in the West Nusa Tenggara province of Indonesia. The 7-km-diameter caldera is open to the NNW.

Tarowa
A geological map by Garvin (2002, shown in Khant et al., 2013) identifies this Tarowa as late Pliocene-early Pleistocene. This volcano is in the center of Sumbawa and includes an eroded caldera about 3.5 x 5 km, open to the SSW.

Lompobatang
Sulawesi
Lompobatang, located at the southern tip of Sulawesi, is a Pleistocene volcano whose products range from 2.3 to 0.8 Ma in age. Two rock suites dominate these products: 1) Potassic alkali basalts, trachybasalts, and trachyandesites, and 2) more evolved silica-oversaturated lavas such as shoshonites, banakites, and latites (Leterrier et al., 1990). Lompobatang is large and relatively well-preserved, with an elevation of 2860 m and a basal diameter of about 55 km (Leterrier et al., 1990).

Kawio Barat
Sangihe Islands
The conical submarine Kawio Barat volcano sits just W of the Sangihe volcanic arc between Sulawesi Island in Indonesia and Mindanao Island in the Philippines. Many of the Sangihe islands contain active volcanoes that have erupted within the last 100 years (including Ruang, Karangetang, Banua Wuhu, and Awu). Satellite imagery showed submarine vents generating visible hydrothermal activity on the W side of the arc. A detailed survey was conducted in June 2010.

Lipang
Sangihe Islands

Napo Taroare
Sangihe Islands

Kawalusu

North Kawio
The North Kawio volcano is a large primarily submarine edifice with multiple peaks, including the islands of Marore (Maru), Kawio, and Kamboreng.

Hamiding
Halmahera
Hamidang volcano is mapped as Quaternary (Supriatna 1980). Based on the morphology of the area, it appears to consist of approximately a dozen small cones.

Tawau Hills
Borneo
The Tawau Hills is a large Miocene to late-Pleistocene volcanic field on the Semporna Peninsula in the NE part of the island of Borneo co. It is in the Malaysian province of Sabah, across Port Cowie bay from the the Indonesian province of Kalimantan. Tahir et al. (2010) noted that the larger mountains resulted from Pleistocene dacite eruptions on top of older andesites; late Pleistocene olivine basalt lavas originated from multiple small cones (eg. Tiger Hill, Bombalai Hill, and Quoin Hill). Two young lava flows from Bombalai extend almost to the coastal plain; they were considered younger than a lava flow radiocarbon dated at about 27,000 years before present (Kirk, 1968), but later workers make no mention of Holocene activity. The lavas from the Tawau area are geochemically distinct from those erupted from fissures at Mostyn (Macpherson et al., 2010), also on the Semporna Peninsula about 30 km NE.

Mostyn
Borneo
Fissure vent(s) ?
Late Quaternary lavas (Kirk 1968).

Usun Apau Plateau
Borneo
Included in Quaternary volcano list (Latter, 1975b), no additional information.

Linau-Balui Plateau
Youngest flow is Quaternary (Kirk, 1968).

Bukit Kajang Plateau
Mapped as Quaternary (Kirk 1968)

Nuit
Included in Quaternary volcano list (Latter, 1975b), no additional information.

Jolo
Sulu Islands
Numerous pyroclastic cones and craters dot 60-km-wide Jolo Island at the SW end of the Philippines archipelago. Jolo lies in the Sulu archipelago, about 150 km SW of the tip of the Zamboanga Peninsula on SW Mindanao Island. Youthful-looking Tumatangus volcano forms the high point of the island. Bud Dajo (or Buddajo) is a basaltic cinder cone that reaches above 600 m elevation; other nearby cones are Matanding, Guimba, and Sungal. Hot springs have been reported at craters on Cagayan Sulu, and solfataras at Siit Lake. A reported eruption in 1641 actually reflected ashfall from the eruption of Parker volcano on Mindanao. A pair of large earthquakes (M 7.4-7.5) on 20-21 September 1897 caused a significant tsunami and later speculation of a possible submarine eruption, but there were no direct observations or later evidence of volcanism.

Balatukan
Mindanao
Compound
Balatukan (also known as Balingoan or Balatocan) is a massive compound stratovolcano that rises above the SW shore of Gingoog Bay in north-central Mindanao, opposite Camiguin Island. Lava flows on its flanks have Pleistocene ages. Although the volcano currently displays fumarolic activity, it is extensively eroded and the age of its latest eruption is not known.

Paco-Maniayao
Mindanao
Located at the NE tip of Mindanao, the Paco-Maniayao volcanic complex is truncated by two nested calderas, 2.5 and 5 km in diameter. The basaltic-dacitic volcano is located east of the N-S-trending Philippine Fault that cuts across eastern Mindanao. Andesitic lava domes rim a breached crater, and the youngest dated rock is an overlying basaltic lava flow dated at about 90,000 yrs +/- 40,000 years BP. Legends record a major caldera collapse eruption (Wolfe 1982, pers. comm.). The age of the last eruption is not known, although the volcano currently displays fumarolic activity. Geological mapping by Omac and Fermin (2012; see Africa et al., 2015) indicated that the youngest volcanics were late Pleistocene.

Blit
Mindanao
Mt. Blit, a poorly known volcanic complex in south-central Mindanao, south of Cotabato City, has two main summits. The youngest dated rocks of the basaltic-to-dacitic volcano, also known as Blik, are about 760,000 years old.

Quezon
Low basaltic to andesitic lava domes at Quezon, north of the Cotabato Basin and east of Illana Bay, were dated at about 115,000 yrs BP.

Kitabud
A lava flow from the Kitabud Mountains, south of Ragang volcano, was dated at about 460,000 yrs BP.

Ampiro
Stratovolcano?
Ampiro volcano lies north of Malindang volcano in NW Mindanao. Ampiro was classified as "active" by Sajona et al. (1994), although it appears on the "inactive" list of PHIVOLCS (2004-). Samples from the flanks of the volcano were dated at between about 700,000 and 290,000 yrs BP.

Imbing
Mount Imbing is one of the highest of a group of volcanoes at the southern end of the SE-most peninsula of the Zamboanga Peninsula. A K-Ar date of 0.82 million years from a sample on the western coast of this peninsula (Sajona et al., 1994, 1997).

Kaladis
K-Ar dates of about 1.08 and 1.21 million years were obtained from a lava flow from Mt. Kaladis on the Zamboanga Peninsula (Sajona et al., 1994, 1997).

Nelangaapan
Central Philippines
This volcanic edifice was mapped at the SE tip of Panaon Island; a K-Ar date of 1.61 +/- 0.08 million years was obtained from a sample.

Ilihan
Central Philippines
Ilihan is Quaternary volcano with a lava flow dated at about 1.24 million years lies in SE Leyte Island, north of Cabalían volcano (Sajona et al., 1997). Another undated Quaternary volcano was mapped immediately to the north of Silago.

Cancajanag
Central Philippines
Cancajanag is a lava dome complex on Leyte Island, north of Mahagnao volcano on the lower NW flank of Lobi. The age of its most recent eruptions is not known, but it was classified as potentially active by PHIVOLCS.

Alto
Compound
The massive compound Alto volcano at the northern end of Leyte Island has K-Ar dates of 0.43-0.38 million years and contains the Tongonan geothermal field.

Maripipi
Maripipi is a small island volcano located NW of Biliran Island. The age of its most recent eruptions is not known, but PHIVOLCS classified it as potentially active.

Hingatungan
Undated Quaternary volcano mapped as Quaternary immediately N of Silago (Sajona et al., 1997).

Lobi
Mapped as Quaternary by Sajona et al. (1997). Listed as inactive by PHIVOLCS.

Pacdahauan
Volcanic features mapped as Quaternary by Sajona et al. (1997) on the Leyte Island peninsula south of Biliran Island.

Amorong Group
Luzon
Mount Amorong is the only one of a cluster of small trachyandesitic lava domes and diatremes at the northern end of the Luzon Central Plain that displays solfataric activity (Wolfe 1982, pers. comm.). A K-Ar date of about 1.14 million years was obtained from the Amorong group, which lies along the Eastern Bataan volcanic lineament. Yumul et al. (1999) collectively called Amorong, Mount Balungao, and Mount Cuyapo the Paniqui Plugs, and noted that nearby Mount Bangcay was a tuff cone.

Santo Tomas
Luzon
Santo Tomas is a stratovolcano with numerous volcanic vents and fissures (Philippines Commission of Volcanology, 1981). There was a report of an eruption or "displacement" in the region on 4 January 1641, described as an outburst of water accompanied by an earthquake. That is also the date of the major eruption of Parker volcano in southern Mindanao that impacted much of the Philippines. The Asin Hot Springs are about 12 km NNW of the summit, but their connection to the volcano is unknown.

Gate Mountains
Luzon
The andisitic-to-rhyolitic Gate Mountains at the southern tip of Luzon Island have K-Ar dates ranging from 2.16 to 0.8 million years.

Sangay
K-Ar dates of about 0.556 to 0.387 million years were obtained from Sangay volcano, which lies NE of Iriga volcano and NW of Malinao volcano.

Cone-Culasi
The Cone-Culasi volcanic field covers an area of about 270 km2 to the W of San Miguel Bay and SE of Labo volcano. K-Ar dates of about 1.21-0.83 Ma have been obtained from this andesitic-to-dacitic volcanic field.

Labo
Compound
Mount Labo is a compound volcano at the NW end of the Bicol Peninsula in SE Luzon, SW of the city of Daet. The forested 1544-m-high andesitic stratovolcano is surrounded by numerous andesitic-to-dacitic satellitic lava domes. Mid-Pleistocene eruptions beginning about 580,000 years ago formed lava domes on the northern side of the complex. The present edifice was formed beginning about 270,000 years ago, and flank lava dome emplacement took place from about 200,000 to about 40,000 years ago. The latest activity from Mt. Labo produced pyroclastic flows from the summit cone about 27,000 years ago. Thermal activity in the form of hot and warm springs continues, and Mount Labo has been the object of an extensive geothermal exploration program.

Dagit-Dagitan
Dagit-Dagitan is an andesitic volcano forming the small Verde Island between Luzon and Mindoro Islands. The most recent activity on Verde Island is probably late Pleistocene in age (Wolfe and Self, 1983) and formed a small tuff cone. No hot springs are present, although wells are hot and argillic alteration is taking place (Wolfe 1982, pers. comm.).

Panay
Mount Panay is a low andesitic stratovolcano on the Calumpang Peninsula west of the Batangas Bay, south of Lake Taal. Panay was mapped as Pleistocene in age by the Philippine Bureau of Mines (Wolf and Self, 1983), but displays strong solfataric activity. Batangas Bay lies at the intersection of two major regional trends, the Bataan Lineament and the Palawan-Macolod Lineament, and may represent a submarine caldera.

Malinao
Forested Malinao stratovolcano, NNW of Mayon, contains a large summit crater that is breached to the east. This Quaternary volcano, also known as Buhi or Takit, was active from about 500,000 to 60,000 years ago (Nielson et al., 1996), but the E flank is the site of Luzon's largest solfataras and hot springs, some of which deposit silicious sinter. A minor explosion from the Naglabong thermal area that ejected blocks in 1980 was probably due to water drawdown during development of the Tiwi geothermal field (Newhall 1994, pers. comm.).

Malepunyo
Malepunyo is an andesitic stratovolcano located east of Taal volcano. K-Ar dates ranging from 3.0 to 0.58 million years were obtained from Malepunyo.

Anilao Hill
Anilao Hill is a basaltic scoria cone east of Taal volcano and SW of Malepunyo volcano. A K-Ar date of about 0.87 millions years was obtained from Anilao Hill.

Cariliao
Cariliao volcano, also known as Mt. Talamitan, is an andesitic stratovolcano located NW of Taal volcano. A K-Ar date of about 1.34 million years was obtained from Cariliao.

Corregidor
Corregidor is a largely submarine caldera with a post-caldera dacitic lava dome located on the Bataan lineament at the mouth of Manila Bay. Corregidor Island forms the northern part of the caldera, and Caraballo Island lies on the SE part of the caldera rim. A radiometric date of 1.0 +/- 0.09 million years was obtained from Corregidor.

Matarem
North of Luzon
Radiometric dates for Matarem (Mafarem) volcano at the SW end of Bataan Island range from about 6 to 1.71 million years (Richards et al., 1986).

Leizhou Bandao
Southeast Asia
The Leizhou Bandao volcanic field is an area of extensive Quaternary lava flows and basaltic cones on the Leizhou (Liuchow) Peninsula in SE China, across the Qiongzhou strait N of Hainan Island. The field is the northern portion of the Qionglei volcano group (also known as the Leiqiong volcanic field), a 7300 km2 basaltic-to-basanitic plateau that covers the southern Leizhou (Liuchow) Peninsula and extends across a broad area of northern Hainan. Volcanism on the peninsula was controlled by E-W extension related to the opening of the South China Sea Basin. Yingfengling and Tianyang are Pleistocene stratovolcanoes that contain large amounts of mantle xenoliths. Many cones are found in the southern portion of the peninsula, and another similar area lies at the the northern end, W of Zhanjiang City. No Holocene features have been identified in either of the volcanic areas on the Leizhou Peninsula.

Lower Chindwin
Southeast Asia
The Lower Chindwin area contains seven or eight late-Pliocene and Pleistocene explosion craters. A lake-filled crater located at Songyuang is surrounded by olivine basaltic lava flows and pyroclastic material. This region along the lower Chindwin River also contains rhyolitic, dacitic, and andesitic rocks. Although some workers have made statements about the presence of Holocene or "sub-Recent" basalts, there is no clear morphological or dating evidence of such activity.

Gaojianshi
Southeast Asia
Late-Cenozoic Gaojianshi volcanoes are located in the Xisha Islands (Wei et al. 1988).

Weizhoudao
Circular, shield-like 4 x 5 km island with a 1 km explosion crater on the south side, of Pleistocene ? age (Whitford-Stark 1987). Part of Qionglei Volcano Group.

Group of 4 volcanoes (IAVCEI).

Group of 3 volcanoes (IAVCEI).

Vinkh-Linkh

Ban Chay
This large area of basalt (200 km2) immediately NE of the Boleo Volcanic Field was described by Whitford-Stark (1987, citing Lacombe, 1969) as having lavas that appear to have flowed radially away from a vent in the S-central portion of the field.

Pleiku-Bantour Volcanic Field
Extensive volcanic area with a number of volcanic edifices (most of which are poorly preserved. IAVCEI 1973 & Whitford-Stark 1987 list as Pleistocene (Whitford-Stark).

Darlac Volcanic Field
Darlac is southern extension of Pleiku-Bantour Volcanic Field.

Bas Song Be
Basaltic field 25 km in diameter (Whitford-Stark 1987).

Pailin
Lavas dated at 1.99 +/- 0.19 million years ago (Whitford-Stark 1987).

Cham

Chup
Lower Pleistocene aged basalts (Whitford-Stark 1987).

Snoul
Lower Pleistocene aged basalts (Whitford-Stark 1987).

Haut Song Be

Bokeo Volcanic Field
Activity continued during mid & recent Quaternary (Whitford-Stark).

Bolaven Plateau
Basalt dated at 1.10 +/- 0.9 million years ago (Whitford-Stark 1987).

Buriram
Basalt flow from a central vent Potassium-Argon dated 0.92 +/- 0.30 million years ago.

Chanthaburi
Potassium-Argon age date of 0.44 million years ago for Khao Phloi Waen cone. Basalt E of Chanthaburi fission track dated at 2.57 million years ago (Whitford-Stark).

Lampang
Flows overlie gravel deposits containing pebble tools. Fission track and Potassium-Argon age dating yield Pleistocene age of 0.64 to 0.95 million years ago (Whitford-Stark 1987).

Ban Chiang Khian
Dissected lava flows dated 1.62 +/- 1.25 million years ago (Whitford-Stark).

Ban Hui Sai
Alkali olivine basalts form dike-like bodies in the Mekong River and a Potassium-Argon age of 1.74 +/- 0.12 million years ago has been obtained from a subcircular outcrop of basanite (Whitford-Stark 1987).

Kuantan Basalt
Basaltic lava flows crop out over an area of 150 km2 near the coast of the South China Sea at Pantai Batu Hitam and Beserah. Bignell and Snelling (1977) obtained a K-Ar age of 1.6 +/- 0.2 Ma.

Medaw Island
Plateau of basalt probably of late Tertiary to sub-Recent age (Whitford-Stark 1987).

Thaton
Rhyolites and rhyolitic tuffs of late Pliocene to Pleistocene age are found at Thaton (Whitford-Stark 1987).

Namyong
Pliocene to Pleistocene basalts to rhyolites erupted from fissure vents (Whitford-Stark 1987).

Tsaolingshan
Taiwan
Tsaolingshan volcano was active during the late Pleistocene (Wang et al., 1999).

Chilung Group
Taiwan
The Chilung volcano group (also spelled Keelung) is of Pleistocene age (Ho, 1988; Wang et al., 1999).

Pengchiahsu
Taiwan
Pengchiahsu is one of five small Pleistocene volcanic islands NE of Taiwan. The summit of the andesitic island (also known as Agincourt) reaches only 129 m above sea level. The age of volcanism is considered to be Pleistocene, but it was reported to display fumarolic activity (Volcanological Society of Japan, 1971). However, there are no more recent reports of fumaroles or other indications of ongoing unrest as of 2015, and the Central Geological Survey makes no mention of them, though it does for other locations.

Huapinghsu
The island of Huapinghsu is thought to be of Pleistocene age (Ho, 1988).

Mienhuayu
Meinhuayu was active from about 0.5 to less than 0.1 million years ago (Wang et al., 1999).

Kogajajima
Ryukyu Islands and Kyushu
The small volcanic island of Kogajajima (Little Gaja Island), about 20 km WNW of Nakanoshima, has andesitic lava domes that were considered to be of late-Pleistocene to Holocene age (Nakano et al., 2001-), and a K-Ar date of 28 +/- 6 ka was reported by Matsumoto et al. (2006). Hydrothermal alteration along with several fumaroles and hot springs were noted during fieldwork in 2005 and 2006 by Nakano and Geshi (2008).

Kobi-sho
Ryukyu Islands and Kyushu
Kobi-sho is a stratovolcano, the top of which breaches the surface of the East China Sea to form a small 1-km-wide island. A few craters are present, but thin basalt flows make up the majority of the island. These basalts are typically porphyritic, characterized by phenocrysts of plagioclase (dominant), olvine, and clinopyroxene (Shinjo, 1998). It was probably active less than a few tens of thousand years ago, but is generally less than 0.2 million years old (Nakano et al., 2001; Shinjo, 1998).

Gajajima
Ryukyu Islands and Kyushu
The andesitic Gajajima stratovolcano lies east of the main arc Ryukyu arc, 30 km WNW of Nakanoshima. The age of the volcano is mid-Pleistocene (Nakano et al., 2001-, mistranslated in the English version as late-Pleistocene to Holocene). Kogajajima (Little Gaja Island) lies 8 km ESE.

Tokara Hirase
Takara Hirase is a group of small islets along a NE-SW trend NE of Kuchino-shima. The highest islet reaches 27 m above sea level above a 600-m-high submarine rise. The rocks are altered but were considered of probable Quaternary age (Nakano et al., 2001-).

Kuroshima
Kuroshima is located in the back-arc region of the Northern Ryuku Arc Segment. It has been K-Ar dated at 1.03 +/- 0.13 million years ago (Ono et al. 1981; Shinjo et al., 2000). Other than the large amount of limestone on the island, Kuroshima is a basaltic-andesitic stratovolcano characterized by an abundance of parasitic monogenetic cinder cones (Joshima et al., 1978; Shinjo et al., 2000).

Satsuma Maru-yama
The Satsuma Maru-yama andesitic lava dome was dated at about 0.5 Ma (Nakano et al., 2001-).

Imuta
Early Pleistocene lava domes (Ono et al., 1981).

Hokusatsu
Hokusatsu erupted expansive plateau lavas ranging from 100-200 m in thickness (Hosono et al., 2003). Lava compositions mostly range from basaltic to andesitic. While silicic deposits were produced throughout Hokusatsu's eruptive history, they mostly dominate the youngest products. Hokusatsu lavas are Plio-Pleistocene in age, ranging from 0.35 to 3.4 Ma (Nakano et al., 2001; Hosono et al., 2008). They are calc-alkaline in composition (Hosono et al., 2008). The Hokusatsu volcanic region is also noted for its silver and gold deposits and is therefore of economic importance to Japan (Hosono et al., 2008).

Sendai
Fission track age dated at 1 million years ago (Ono et al., 1981).

Sone
A basaltic scoria cone lies along the W coast of the northern peninsula of Nakadori-jima of the Goto Islands off the western coast of Kyushu (Nakano et al., 2001-). It is described in the GSJ database (2015) as an isolated monogenetic volcano distinct from the Ojikajima volcano group to the N, with the most recent activity in the middle Pleistocene (0.19 Ma). It is designated as a natural monument, Sone volcano "red fired cliff" after the a cliff face along the bay to the SW from the summit. The villages of Sonego and Sone lie on the NW flank of the cone.

Ojikajima
Ojikajima is a field of monogenetic cinder cones located about 200 km behind the active volcanic front (Sudo et al., 1998). Ojika-Jima itself is a shield volcano forming a relatively flat island about 36 km2 in area, containing a variety of small peaks and pyroclastic cones ranging from 50 to 110 m in height (Sudo et al., 1998; Nakano et al., 2001). The products of this volcanic group, considered to be cogenetic, are predominantly scoria deposits and lava flows (Sudo et al., 1998). The scatter of small islands surrounding Ojika-Jima are considered part of the Ojikajima Volcanic Group as well (Sudo et al., 1998). The 1.3-1.1 Ma Uku-jima stratovolcano occupies an island to the north (Nakan et al., 2001; Sudo et al.,1998). Based on K-Ar ages (Nakano et al., 2001; Sudo et al., 1998) and the local geology, the eruptive history is divided into four stages: 1 (1.1-0.85 Ma): the most voluminous eruptive phase, with activity concentrated at the center of the field; 2 (0.85-0.7 Ma): after a possible volcanic hiatus between 0.95 and 0.76 Ma, activity resumes in the center of the field; 3 (0.7-0.56 Ma): volcanic activity expands to the adjacent eastern and western islands; 4 (0.56-0.3 Ma): volcanic activity continues but at a lower intensity (Sudo et al., 1998). Volcanism in this field is likely a result of a mantle diapir (Sudo et al., 1998).

Taradake
Taradake is a stratovolcano and lava dome NW of Unzen volcano that was active mostly between 1.3 and 0.4 million years ago (Nakano et al., 2001). Mainly basalt was erupted from about 4.6 to 1 Ma. At this point, a stratovolcano formed, erupting calc-alkaline andesites and dacites. Basaltic volcanism resumed at around 0.8 Ma, and from 0.6 to 0.4 Ma was mostly andesitic lavas (Higo and Mashima, 2004).

Kakuto
Kakuto is a large figure-eight shaped caldera north of Kirishima that consists of the overlapping Kakuto and Kobayashi calderas, formed about 0.4-0.5 and 0.3 Ma, respectively (Nakano et al., 2001-). Major explosive eruptions have occurred around 110,000, 65,000 and 12,000 years ago (Newhall and Dzurisin, 1988).

Kinpo
The Kinpo-san stratovolcano and lava dome were active from about 1.4 to 0.18 million years ago (Toshida et al., 2006). In total it is about 150 km2 in area and comprised of four main cones and some "parasitic" lava domes (Yanagi et al., 1988). Deposits mainly consist of andesitic lava flows and pyroclastics, the latter of which are more heavily dissected (Yanagi et al., 1988).

Yabakei
The largely buried Yabakei caldera (also known as the Shishimuta caldera), a member of the Hohi Volcanic Zone, was the source of two major Pleistocene explosive eruptions producing the dacitic Yabakei (0.1 Ma) and Imaichi (0.9 Ma) pyroclastic flows (Hayashida et al., 1996; Kamata, 1989). The Yabakei pyroclastics take the form of densely welded tuffs, originally more than 110 km3 in total volume, and crop out over an area of about 480 km2 (Kamata, 1989). The 8-km-diameter funnel-shaped caldera is filled with breccia and shows no evidence of resurgent volcanic activity after these two caldera eruptions. However, post-caldera monogenetic activity appears to have continued for about 600,000 years after the caldera activity (Kamata, 1989).

Hane-yama
Hane-yama and Kameishi-yama are rhyolitic and dacitic volcanoes dated between 0.6 and 0.5 million years (Nakano et al., 2005).

Hohi
The Hohi volcanic group was Potassium-Argon age dated at about 600,000 - 400,000 years (Nakano et al., 2001-).

Futago
The Futago volcano group consists of several lava domes and a lava plateau with ages of 1.5-1.1 million years forming a peninsula NE of Beppu City (Nakano et al., 2001-).

Hime-shima Volcanic Group
The Hime-shima volcano group north of the northern coast of Kyushu consists of lava domes and pyroclastic cones active from 350,000 to 20,000 years ago (Nakano et al., 2001-).

Kurose
Volcanic remnant
Small basaltic islets forming a volcanic neck rise only 8 m above sea level north of Genkaijima off the NW coast of Kyushu and are dated at about 1.13 +/- 0.12 million years (Nakano et al., 2001; Yokochi et al., 2005). Kurose is actually a small reef, formed from a highly eroded lava flow and columnar basalts (Yokochi et al., 2005). It is known for its ultramafic xenoliths, rich in olivine and pyroxene, which have been extensively studied geochemically for insight into the origin of these back-arc magmas (Senda et al., 2007).

Iki Volcanic Group
A group of pyroclastic cones of Iki Island NW of Kyushu was active from the Pliocene to about 600,000 years ago (Nakano et al., 2001). However, volcanic activity in the Iki Islands began as much as 15 Ma as the Japan Sea back-arc basin began to open, producing mostly basaltic lavas (Kimura et al., 2005). The Iki volcanic group is part of a Quaternary alkaline province in northwestern Kyushu; the volcanic products range from basaltic to rhyolitic (Aoki and Oji, 1966).

Mutsure-jima
Honshu
A lava flow dated at about 1.2 million years forms Mutsure-jima island just off the SW tip of Honshu (Nakano et al., 2001-). Kifune volcano (1.6 or 1.3 million years old), 7 km to the east, consists of basaltic scoria cones and lava flows.

Shikuma
Honshu
Shikuma volcano consists of Shikumaga-take (dated at about 450,000 years ago) and Dake-yama lava domes (Nakano et al., 2001-).

Tokuyama-Mitake
Honshu
Tokuyama-Mitake is a lava dome in SW Honshu dated at about 0.43 million years (Nakano et al., 2001-). It is also known as Mitake-yama or Kinpo-san.

Sengoku
The Sengoku volcano group consists of a group of four mid-Pleistocene lava domes active from about 0.5 to 0.36 million years ago (Nakano et al., 2001-).

Chojagahara
Chojagahara is a 1.7 million year old pyroclastic cone and lava flow (Nakano et al., 2001-).

Aonoyama
The Aonoyama volcano group consists of about 10 lava domes from about 1.3 to 0.15 million years in age (Nakano et al., 2001-). The volcanic products have a narrow chemical composition similar to that of Daisen and consist of biotite and hornblende andesites that often contain granulitic inclusions (Matsuhisa and Kurasawa, 1983).

Oetaka-yama
Oetake-yama consists of a group of lava domes active from about 1.8 to 0.8 million years ago (Nakano et al., 2001-). Kano and Takarada (2007) noted late-Pliocene to early Pleistocene activity, including at the early Pleistocene Sen-yama pyroclastic cone north of the Oetaka-yama (O'e-Taka-yama). The latest activity noted was K-Ar dated at about 1.8-1.6 million years.

Yokote
The Yokote volcano group was active between about 2.3 and 0.9 million years and consists of 10 monogenetic volcanoes (Nakano et al., 2001-).

Noro
The Noro basaltic lava flow was erupted about 1.1 million years ago from a monogenetic volcano (Nakano et al., 2001-).

Daikon-jima
A scoria cone and lava flow at Daikon-jima was erupted about 250,000 or 200,000 years ago (Nakano et al., 2001-).

Tsuruta
The Tsuruta volcano group consists of a group of scoria cones about 1.2 million years in age aligned NW-SE, including the Takatsuka-yama cone (Nakano et al., 2001-).

Daisen
Daisen volcano overlooking the Japan Sea has been the source of large explosive eruptions during the late Pleistocene. The last dated major eruption took place about 17,000-18,000 years before present, but at least one large tephra deposit is younger (Machida and Arai, 1992). Although included in a list of volcanoes with eruptions in the past 2000 years (Hayakawa, 1994a), the list includes some youthful volcanoes that are not Holocene in age, and the latest eruption of Daisen occurred during the late Pleistocene (Hayakawa 1996, pers. comm.). The volcanic products mostly consist of biotite and hornblende andesites (Matsuhisa and Kurasawa, 1983).

Ogino-Sen
The Ogino-Sen volcano group in eastern Tottori Prefecture consists of 20 monogenetic volcanoes from 1.2 to 0.4 million years in age (Nakano et al., 2001-). The adjacent Mikata volcano group in western Hyogo Prefecture consists of 8 monogenetic volcanoes from 1.7 to 0.22 million years in age.

Kannabe
The Kannabe volcano group is the westernmost and youngest of a cluster of monogenetic volcanoes that are part of the Kita-Tajima volcano group in Hyogo Prefecture, along with Mesaka, Kamisano, and Gembudo volcanoes. A radiocarbon age of 19,000 years before present was obtained from the small shield volcano of Kannabe-yama (Ono et al., 1981), and Nakano et al (2001-) listed an age of 20,000 or 10,000 years. Mesaka volcano was dated at 130,000 years, Kamisano volcano at 230,000 years, and Gembudo (Genbudo) at about 1.6 million years (Nakano et al., 2001-). Other more isolated volcanoes of the Kita-Tajima volcano group, such as the Ogino-Sen and Mikata volcano groups and Takara-yama, are listed separately in this compilation.

Takara
Takara-yama (also known as Takura-yama) is a small shield volcano topped by a pyroclastic cone and was active about 0.4 or 0.3 million years ago (Nakano et al., 2001-). It is the SE-most volcano of the Kita-Tajima volcano group in SW Honshu.

Nanzaki
Nanzaki (also known as Ikenohara) is a basaltic pyroclastic cone at the southern tip of the Izu Peninsula dated at about 450,000 or 400,000 years (Nakano et al., 2001-).

Jaishi
Jaishi-yama is a small andesitic shield volcano with a lava flow dated at about 1.4-1.3 million years (Nakano et al., 2001-).

Tanaba
Tanaba-yama is an andesitic stratovolcano dated at about 1.5-1.2 million years (Nakano et al., 2001-).

Daruma
Daruma-yama is an andesitic stratovolcano dated at about 0.8-0.5 million years (Nakano et al., 2001-). Ida volcano and the underlying Osezaki volcano lie to the north at the NW tip of the Izu Peninsula.

Tenshi
Tenshi is an andesitic and dacitic stratovolcano dated at about 1.7-1.4 million years (Nakano et al., 2001-).

Usami
Usami is a basaltic-to-andesitic stratovolcano north of the Izu-Toba volcano group dated at about 0.9 to 0.4 million years (Nakano et al., 2001-).

Taga
Taga is an basaltic-to-andesitic stratovolcano SW of Atami City dated at about 0.7-0.3 million years (Nakano et al., 2001-).

Yugawara
Yugawara is an andesitic and basaltic stratovolcano south of Hakone volcano dated at about 0.4-0.2 million years (Nakano et al., 2001-).

Ashitaka
Ashitaka-yama is a large basalitic-to-dacitic stratovolcano and lava dome SE of Fuji volcano that was active from about 0.4-0.1 million years ago (Nakano et al., 2001-).

Kirigamine
Kirigamine is a small shield volcano and lava dome (Wada-Toge) that lies west of Kita-Yatsugatake volcano and NW of Yatsugatake volcano. Kirigamine was active about 1.3-0.75 million years ago (Oikawa and Nishiki, 2005).

Utsukushigahara
Utsukushigahara, NE of Yatstuga-take, was active about 1.6-1.2 million years ago (Nakano et al., 2001-).

Ueno
Ueno volcano is a small basaltic-to-andesitic shield volcano and lava flow that was active about 1.6 or 1.5 million years ago (Nakano et al., 2001-). Ono et al. (1981) listed a Potassium-Argon date of <110,000 thousand years ago.

Yuga-mine
Yuga-mine is a rhyolitic lava dome SW of On-take volcano that was active about 0.1 million years ago (Nakano et al., 2001-).

Kurofuji
The Kurofuji (Black Fuji) lava-dome complex and Kanaga-take and Kayaga-take stratovolcanoes active from about 1 million to 0.4 or 0.2 million years ago lie in Chichibu-Tama National Park north of the city of Kofu (Nakano et al., 2001-).

Yatsugatake
The older Yatsugatake volcano was active about 1 million years ago and the younger was active about 0.2 million years ago (Nakano et al., 2001). This complex of N-S-trending stratovolcanoes extends for about 10 km and is also known as Minami Yatsugatake ("Southern Eight Peaks") (Matsuhisa and Kurasawa, 1983). Both ends of the complex produced volcanic dry avalanche deposits (sector collapses of a volcanic cone), ranging from 0.27 to 9.0 km3 in volume(Tadahide, 1983). The volcanic rocks of the northern end generally consist of hornblende and pyroxene dacites, whereas those at the southern end are composed of olivine and pyroxene andesites. The volcanic products also contain xenoliths derived from a diverse assortment of basement rocks (Matsuhisa and Kurasawa, 1983). Extensive geochemical data is available from Matsuhisa and Kurasawa (1983).

Eboshi-Washigatake
Eboshi and Washiga-take are early Pleistocene andesitic stratovolcanoes active about 1.6-1.1 million years ago (Nakano et al., 2001-).

Bishamon-dake
Bishamon-dake is an andesitic stratovolcano active about 0.4-0.25 million years ago (Nakano et al., 2001-).

Dainichiga-take
Dainichiga-take is an andesitic-to-dacitic stratovolcano that was active about 1.1-0.9 million years ago (Nakano et al., 2001-).

Ryohaku Maru-yama
Ryohaku Maru-yama (named to distinguish from Maru-yama volcano in Hokkaido) is an andesitic stratovolcano active about 0.4-0.3 million years ago (Nakano et al., 2001-).

Gankyoji
Gankyoji-yama is a Pliocene-Pleistocene andesitic stratovolcano active until about 1.3 million years ago (Nakano et al., 2001-).

Kyoga-take
The Kyoga-take volcano group consists of andesitic stratovolcanoes active about 1.4-0.7 million years ago (Nakano et al., 2001-).

Dainichi-yama
Dainichi-yama is an early Pleistocene andesitic stratovolcano west of Haku-san volcano (Ono et al., 1981). This volcano was not listed by Nakano et al. (2001-).

Tomuro
The Tomuro lava-dome complex contains four domes that were active from about 0.4-0.3 million years (Nakano et al., 2001-).

Kamitakara
Kamitakara (or Takara) volcano was the source of deposits forming the Kamitakara pyroclastic flow plateau. The dacitic-to-rhyolitic deposits were erupted about 0.75 or 0.70 million years ago (Nakano et al., 2001-). Ono et al. (1981) listed a Potassium-Argon date of about 600,000 years.

Kaminoroka
Kaminoroka volcano produced andesitic and dacitic lava flows about 0.4-0.2 million years ago (Nakano et al., 2001-).

Hodakadake
Hodakadake, the highest of a rugged group of peaks in the scenic Northern Alps National Park, lies within the Hodaka Graben, the source of two major explosive eruptions about 1.75 million years ago. The eruption of the caldera-forming Nyukawa Pyroclastic Flow Deposit about 1.76 million years ago (Kimura and Nagahashi, 2007) was followed by the Ebisutoge-Fukuda Tephra, with an estimated volume of 380-490 km3 (Kataoka et al., 2001).

Momisawa-dake
Momisawa-dake volcano in the Northern Japan Alps was the source of a dacitic-rhyolitic pyroclastic-flow plateau. The complex includes the Sueindani vent and the Okuhida pyroclastic-flow deposit and was active sometime between about 0.65 and 0.3 million years ago (Nakano et al., 2001-).

Shirouma-Oike
The andesitic and dacitic Shirouma-Oike volcanic complex consists of the Norikura-dake stratovolcano and the Kazafuki-dake lava dome. An older volcano was active 0.8-0.5 million years ago and younger volcano was active since 0.2 million years ago (Nakano et al., 2001-).

Madarao
Madarao-yama is an andesitic-to-dacitic stratovolcano and lava domes that were active about 0.7-0.55 million years ago (Nakano et al., 2001).

Kurohime
Kurohime is a stratovolcano and associated lava domes south of Myoko volcano that were active from about 250,000 to 50,000 years ago (Nakano et al., 2001-).

Iizuna
Iizuna stratovolcano south of Kurohime volcano was active about 0.34-0.15 million years ago (Nakano et al., 2001-).

Motodori
The andesitic Motodori-yama lava dome was active about 0.2 million years ago (Nakano et al., 2001-).

Minakami
Minakami-yama lava dome was active about 0.3 million years ago (Nakano et al., 2001-) and is a post-caldera dome of Matsushiro volcano.

Eboshi
The Eboshi volcano group immediately west of Asama volcano includes a group of andesitic-to-dacitic stratovolcanoes and lava domes that were active about 0.97-0.35 million years ago (Takahashi and Miyake, 2004; Takahashi, 2004).

Hanamagari
The andesitic Hanamagari-yama and neighboring Asamakakushi-yama stratovolcanoes immediately eastd of Asama volcano were active about 1.1-0.7 million years ago (Nakano et al., 2001-).

Azumayasan
Azumayasan is an andesitic stratovolcano and lava dome that was active about 0.9-0.3 million years ago (Nakano et al., 2001-). A plinian eruption took place about 0.3 million years ago.

Omeshi-dake
The andesitic Omeshi-dake stratovolcano west of Kusatsu-Shirane volcano was active about 1.1 million years ago (Nakano et al., 2001-).

Takayashiro
Takayashiro-yama is an andesitic stratovolcano that was active about 0.3-0.2 million years ago (Nakano et al., 2001-).

Sekita
The andesitic Sekita volcano was active about 1.7-1.1 million years ago (Nakano et al., 2001-).

Kenashi
Kenashi-yama is an andesitic stratovolcano active about 1.6-1.0 million years ago (Nakano et al., 2001-).

Torikabuto
The andesitic Torikabuto-yama stratovolcano was active about 0.9-0.7 million years ago (Nakano et al., 2001-).

Naeba
The andesitic Naeba-san stratovolcano and caldera was active about 0.8-0.2 Ma (Nakano et al., 2001-).

Iiji
The andesitic Iiji-san stratovolcano was active about 0.3-0.2 million years ago (Nakano et al., 2001-). The Iiji Moka Pumice was erupted about 0.22-0.23 million years ago.

Masugata
The andesitic Masugata-yama pyroclastic cone and lava flow was active about 1.1 million years ago (Nakano et al., 2001-).

Komochi-Onoko
The Komochi-Onoko volcano group NW of Maebashi City consists of the andesitic Komochi-yama stratovolcano and lava dome on the east and andesitic Onoko-yama stratovolcano on the west. Komochi-yama was active from about 0.9-0.2 million years and Onoko-yama from about 1.3-1.2 million years (Nakano et al., 2001-).

Kinunuma-Nenakusa
The dacitic Kinunuma volcano produced a lava flow and pyroclastic flow about 0.24 or 0.20 million years ago. The Kinunuma-Kurodahara tephra consists of pumice fall deposits (~5 km3) and mostly-welded pyroclastic flow deposits (less than 1 km3), erupted at 0.20-0.24 Ma. Andesitic and dacitic lava domes of the Nenakusa-yama volcano to the SE were active about 0.3 million years ago.

Sukai-Kesemaru
The basaltic-to-dacitic Sukai stratovolcano was active about 1.6-0.9 million years ago (Nakano et al., 2001-). Koshin-zan volcano is part of the Sukai edifice, and activity of the roughly 1-million-year-old Kesemaru-yama volcano to the south overlapped with activity at Sukai-san volcano.

Numanokami
The andesitic Numanokami-yama stratovolcano was active about 1.1 million years ago (Nakano et al., 2001-).

Hotaka
The andesitic-to-dacitic Hotaka-yama volcano (also known as Joshu-Hotaka) was active about 1.2-1 million years ago (Nakano et al., 2001-).

Ayame-daira
The Ayame-daira stratovolcano south of Ozegahara in Nikko National Park was active about 1.6 million years ago (Nakano et al., 2001-). Nikura-yama volcano lies to the SE.

Nyoho-Akanagi
Nyoho and Akanagi volcano consists of a basaltic-to-dacitic stratovolcano and lava dome active about 0.5-0.4 million years ago (Nakano et al., 2001-).

Sunagohara
The rhyolitic Sunagohara caldera and lava dome, east of Numazawa caldera, was active about 0.29-0.22 million years ago (Nakano et al., 2001-). The Sunagohara-Kubota tephra is made up of pumice fall deposits (ca. 4 km3 in volume) and pyroclastic flow deposits (more than 2 km3 in volume), erupted from Sunagohara caldera at about 0.22Ma.

Nekoma
The andesitic Nekoma volcano, immediately W of Bandai, was active about 1-0.8 million years ago (Nakano et al., 2001-). The caldera is about 3 km in diameter and contains a lake on the western side.

Futamata
Futamata-yama is a late Pleistocene (about 140,000 or 90,000 years old) stratovolcano and lava dome (Nakano et al., 2001-). A thick lava flow extends to the NW. It is located within the Quaternary Tonohetsuri caldera (Yamamoto, 1995; 2007). The oval-shaped Narioka caldera cuts the western rim of Tonohetsuri caldera and the western rim of the older Ono caldera. These large calderas were formed during eruption of the Kumado, Ashino, and Nishigo pyroclastic flows about 1.4, 1.2, and 1.0 million years ago, respectively.

Aizu Nunobiki
Aizu Nunobiki-yama is an andesitic-to-dacitic stratovolcano that was active about 1.4 million years ago (Nakano et al., 2001-).

Asakusa
Asakusa-dake is an andesitic-to-dacitic stratovolcano active about 1.7-1.5 million years ago (Nakano et al., 2001-).

Sumon
Sumon volcano is an andesitic stratovolcano active about 2.4-1.7 million years ago (Nakano et al., 2001-). The main part of the edifice of Sumon-dake was constructed during the early Quaternary.

Aoso
Aoso volcano is an andesitic-to-dacitic stratovolcano at the SE end of the Zao massif. Aoso-yama was active about 0.4-0.3 million years ago (Nakano et al., 2001-). Aoso was constructed within a Pleistocene caldera.

Mukaimachi
Mukaimachi is a dacitic and andesitic caldera with a post-caldera lava dome. Post-caldera activity at Mukaimachi took place about 0.8-0.6 million years ago Nakano et al., 2001-).

Shirataka
Shirataka volcano is an andesitic-to-dacitic stratovolcano NW of the Zao volcanic massif. Shirataka-yama was active about 0.9-0.7 million years ago. Growth of a stratovolcano was followed by emplacement of a pyroclastic flow and growth of lava domes. Late-stage collapse produced a large debris avalanche and formed a 4-km-wide horseshoe-shaped caldera.

Ganto-Kamuro
Ganto and Kamuro volcanoes form the Kita-Zao (North Zao) volcano group. They were active about 0.4-0.3 million years ago (Nakano et al., 2001-).

Adachi
Adachi is a dacitic pyroclastic cone cone that was the source of the Adachi-Medeshima pumice fallout about 80,000 years ago (Nakano et al., 2001-).

Daito
Daito volcano is an andesitic stratovolcano NNE of the Zao volcanic massif. Daito-dake was active about 1 million years ago (Nakano et al., 2001-).

Funagata
The Funagata volcanic complex consists of two basaltic-to-andesitic stratovolcanoes NW of Sendai City. Funagata-yama was active about 0.9-0.5 million years ago and Izumiga-take volcano about 1.5-1.1 million years ago (Nakano et al., 2001-).

Gassan
Gassan is a massive andesitic-to-dacitic stratovolcano south of Chokai volcano that was active about 0.9-0.3 million years ago (Nakano et al., 2001-). Gassan was constructed with a large Pleistocene caldera.

Onikobe
Onikobe caldera, located SW of Kurikoma volcano, is one of the few calderas in Japan with evidence of ring fractures and a resurgent dome. The Takahinata lava dome was last active about 350,000 years ago according to a fission-track date. Onikobe was active until about 0.2 million years ago (Nakano et al., 2001-). Geysers were said to be discovered about 1700 years ago at Onikobe, and geysers and hot springs are present today within the caldera.

Takamatsu
Takamatsu volcano (Takamatsu-dake) is a dacitic stratovolcano active about 0.3 million years ago (Nakano et al., 2001-). Takamatsu was constructed within a Pliocene caldera.

Kobinai
Kobanai volcano (Kobinai-yama) is an andesitic-to-dacitic stratovolcano active about 1-0.6 million years ago (Nakano et al., 2001-).

Yakeishi
Yakeishi volcano (Yakeishi-dake) is an andesitic stratovolcano that was active about 1-0.2 million years ago (Nakano et al., 2001-).

Tazawa
Caldera(?)
Tazawa was considered to be a late-Pleistocene caldera (Japan Assoc. Quat. Res. 1987), however Nakano et al. (2001-) noted that it is uncertain whether the depression was formed by volcanic activity. The elevation listed is that of the surface of Tazawa lake.

Kayo
Early or mid Pleistocene (Japan Assoc. Quat. Res. 1987).

Nyuto-Takakura
The Nyuto-Takakura volcano group consists of Nyuto-san, Takakura-yama, Hiragakura-yama, Marumori, Sankagu-yama, Sasamori-yama, Yumori-yama volcanoes. The basaltic-to-dacitic volcano group was active about 0.6-0.1 million years ago (Nakano et al., 2001-).

Tamagawa
The dacitic and rhyolitic Tamagawa caldera was the source of the Tamagawa Ignimbrite associated with formation of a pre-Yaka-yama caldera. The caldera was active about 2 million and 1 million years ago (Nakano et al., 2001-).

Nanashigure
Nanashigure volcano is a Pleistocene pyroclastic-flow plateau and lava dome. Nanashigure-yama was active about 1.1-0.9 million years ago (Nakano et al., 2001-).

Daira-Komaga-take
Daira-Komagatake is an andesitic stratovolcano active about 0.2 million years ago (Nakano et al., 2001-).

Tashiro
Tashiro-dake is an andesitic stratovolcano and lava dome that is younger than about 0.6 million years (Nakano et al., 2001-).

Moriyoshi
Moriyoshi-zan is a basaltic-to-dacitic stratovolcano and lava dome that was active about 1.1-0.7 miilion years ago (Nakano et al., 2001-).

Kanpu
The small Kanpu stratovolcano lies on the Oga Peninsula along the Japan Sea coast NW of Akita City. It was at one time considered to be Holocene or even historical in age, but later work has shown it to be late-Pleistocene. Accounts of radiocarbon dates of about 2700 yrs BP for a pumice eruption followed by a pyroclastic flow (Hasenaka et al., 1992) have been revised, and the report on the 1810 "eruption" submitted to the Shognate was manufactured by the people of the Akita Clan in Edo (present Tokyo) in order to receive reimbursement for damaged crops. Nakano et al. (2001-) list the age of Kanpu as less than 30,000 years, and Kudo and Hoshizumi (2006-) listed no Holocene eruptions. Kanpu produced mostly andesites (Notsu, 1983).

Okiura
The 15-km-wide Okiura caldera was formed by the eruption of the Aoni Tuff about 1.5 million years ago. Post-caldera volcanoes comprise several lava domes including Kenashi-yama.

Mutsu-Hiuchi-dake
Mutsu-Hiuchi-dake, on the Shimokita Peninsula, is the northernmost volcano on the island of Honshu. The 781-m-high andesitic-dacitic stratovolcano is Pleistocene in age, with dated activity during an interval ranging from about 700,000 to 50,000 years ago, although fumarolic activity continues at the volcano.

Dorobu
The Dorobu caldera, 13 x 6 km in diameter, is located within the southern part of NE Honshu about 10 km W of Takaharayama volcano. Miura and Tamai (1998) note that many other volcanoes formed during the late Miocene-Pliocene are within a 40 x 40 km area known as the Minami-Aizu geothermal field, including Okukinu, Kawaji, Yunishigawa, Tokusa, Yaso, Sannotoge, and Furumachi. Based on K-Ar ages, Dorobu is thought to have been active from the early Pliocene into the Pleistocene (5.59-1.79 Ma).

Udonejima
Izu, Volcano, and Mariana Islands
Udonejima, though techincally part of the Izu Volcanic Arc, is actually considered to be situated just behind the true volcanic front, along a line of volcanoes that is oblique to the Izu Trench. The volcanic rocks of this lineament are characterized by high-alumina basalts, calc-alkaline basalts, andesites, and rhyolites (Onuma et al., 1983). The andesites are rich in pyroxene, and the rhyolites often contain hypersthene, hornblende, and biotite (Onuma et al., 1983).

Inamba-jima
Izu, Volcano, and Mariana Islands

Onoharajima
Izu, Volcano, and Mariana Islands
Onoharajima is considered to be situated behind the true front of the Izu Volcanic Arc, along a line of volcanoes that is oblique to the Izu Trench. The volcanic rocks of this lineament are characterized by high-alumina basalts, calc-alkaline basalts, andesites, and rhyolites (Onuma et al., 1983). Onoharajima is dominated by andesites of calc-alkaline composition (Onuma et al., 1983).

Tracey Seamount
Samples of fresh pumice were dredged from the summit of the conical Tracey Seamount, part of the Quaternary Marianas chain (Corwin, 1971).

Kasuga 3
Kasuga 3 is the southern-most of three volcanoes forming the Kasuga seamount chain, which trends SSW from the volcanic front of the Izu-Marianas arc. Embley et al. (2004) found no evidence of continuing hydrothermal activity.

Eifuku

Nichiyo Seamount
Nichiyo Seamount, one of the Shichiyo Seamounts, named for the seven days of the week ("Sunday"), lies south of Sofugan volcano. No hydrothermal activity or other unrest has been noted here, but it is assumed to be at least Pleistocene.

Getsuyo Seamount
Getsuyo Seamount, one of the Shichiyo Seamounts, named for the seven days of the week ("Monday"), lies south of Sofugan volcano. No hydrothermal activity or other unrest has been noted here, but it is assumed to be at least Pleistocene.

Kayo Seamount
Kayo Seamount, one of the Shichiyo Seamounts, named for the seven days of the week ("Sunday"), lies south of Sofugan volcano. No hydrothermal activity or other unrest has been noted here, but it is assumed to be at least Pleistocene.

Kinyo Seamount
Kinyo Seamount, one of the Shichiyo Seamounts, named for the seven days of the week ("Friday"), lies south of Sofugan volcano. No hydrothermal activity or other unrest has been noted here, but it is assumed to be at least Pleistocene.

Mikura Seamount

Shikaribetsu Group
Hokkaido
Shikaribetsu consists of a group of andesitic-to-dacitic lava domes west and south of Lake Shikaribetsu in central Hokkaido. The youngest domes were constructed along a ENE-WSW line south of the lake. The largest dome, Higashi-Nupukaushinupuri, was built at the SW, breached end of a horseshoe-shaped crater. Two or more large debris-avalanche deposits extend to the south. Although the Japan Association of Quaternary Research (1987) mapped the youngest domes as Holocene, and Nakano et al. (2001-) indicated that the age of the latest eruptions was less than 20,000 years, Hayakawa (2009, pers. comm.) stated that there was no evidence of Holocene eruptions.

E-san Maru-yama
Hokkaido
E-san Maru-yama, an andesitic stratovolcano lying NW of E-san volcano, was active about 0.2 million years ago (Nakano et al., 2001-).

Yokotsu
Hokkaido
Most of Yokotsu-dake volcano formed during the Pliocene, but Nakitsura-yama on the east side was probably constructed during the late Quaternary (Nakano et al., 2001-).

Oshima-Ko-jima
Oshima-Ko-jima, also known as Matsumae-Ko-jima, is an andesitic stratovolcano whose summit forms a small island off the SW tip of Hokkaido (Nakano et al., 2001-).

Oshima Maru-yama
Oshima Maru-yama, a Pleistocene stratovolcano and lava dome near the SW tip of Hokkaido, was active from about 2.5-1.5 million years ago.

Hakodate-yama
Hakodate-yama, a low dacitic stratovolcano, rises above the city of Hakodate in SW Hokkaido.

Zenikame
A 2-km-wide shallow submarine caldera just off the SW tip of Hokkaido, SE of Hakodate City reaches to within 30 m of the sea surface. It was the source of the Zenikame-Menagawa (Z-M) tephra about 33,000-45,000 years ago.

Nigorikawa
The Mori geothermal field is located in the late-Pleistocene Nigorikawa caldera in SW Hokkaido. The small 3-km-wide caldera along the shores of Uchiura Bay WNW of Komagatake volcano, was formed during a major explosive eruption about 12,000 years ago. The caldera-forming eruption included the emplacement of pyroclastic-fall and -surge deposits and pyroclastic-flow deposits that extend north and west to the Pacific coast. The flat-bottomed caldera floor is intersected by roads and houses of the town of Nigorigawa, and a river of the same name drains the caldera to the NE through a notch in the caldera rim.

Okushiri-Katsuma-yama
Okushiri-Katsuma-yama volcano lies at the northern end of Okushiri Island off the SW coast of Hokkaido and consists of three centers, Horonai-gawa caldera, Katsuma-yama and Nishi-Katsuma-yama. They were active about 0.7-0.2 million years ago (Kano et al., 2006).

Kariba
Kariba-yama, an andesitic stratovolcano along the SW coast of Hokkaido, was active about 0.8-0.25 million years ago (Nakano et al., 2001-).

Washibetsu
Washibetsu-dake volcano, an andesitic stratovolcano SE of Usu volcano, was active about 0.5 million years ago (Nakano et al., 2001-).

Akaigawa
Akaigawa, a late-Pliocene double caldera containing several somma volcanoes, was active about 1.7-1.3 million years ago (Nakano et al., 2001-).

Shiribetsu
Shiribetsu volcano, located immediately SE of Yotei volcano in southwestern Hokkaido, is a small, 1107-m-high andesitic stratovolcano that contains a 1.5-km-wide crater breached widely to the west. It was created by a massive debris avalanche that removed the summit and swept more than 7 km to the west, forming a hummocky deposit at the SE foot of Yotei volcano. Shiribetsu volcano was mapped as Holocene in age (Japan Association of Quaternary Research, 1987), however Nakano et al. (2001-) list its age as several hundred thousand years.

Orofure-Raiba
The Orofure-Raibe volcano group consists of Orofure-yama and Raibe-dake andesitic stratovolcanoes lying immediately west of Kuttara volcano. They were active about 0.6 million years ago (Nakano et al., 2001-).

Horohoro-Tokushumbetsu
The andesitic Horohoro-yama and Tokushumbetsu volcanoes were active about 0.7 or 0.6 million years ago (Nakano et al., 2001-).

Raiden
The Raiden-yama volcano complex along the SW coast of Hokkaido consists of Raiden-yama, Iwanai-dake and Mekunnai-dake volcanoes and was active about 1.4-0.8 million years ago (Nakano et al., 2001-).

Soranuma
Soranuma, a small andesitic shield volcano and lava flow, was active about 0.8 million years ago (Nakano et al., 2001-).

Sapporo
Sapporo volcano (Sapporo-dake), a small andesitic shield volcano and lava flow, was active about 0.8 million years ago (Nakano et al., 2001-).

Tomuraushi Volcanic Group
The andesitic-to-dacitic Tomuraushi) volcano group located between Tokachi and Daisetsu volcanoes consists of a half dozen stratovolcanoes and lava domes that were active about 1.1-0.1 million years ago (Nakano et al., 2001-).

Chubetsu
Chubetsu volcano (Chubetsu-dake or Tyubetu-dake), an andesitic stratovolcano SE of Daisetsu volcano, was active about 1-0.8 million years ago (Nakano et al., 2001-).

Tokachi-Eboshi
The Tokachi-Eboshi volcano group consists of several lava domes and volcanic necks that were active about 1.8-0.7 million years ago (Nakano et al., 2001-).

Niseikaushuppe
The basaltic Niseikaushuppe-dake stratovolcano was active about 1.1 million years ago (Nakano et al., 2001-).

Tengu-Hirayama
The Tengu-Hirayama volcano group consists of the andesitic-to-dacitic Tengu and Hira-yama volcanoes. They were active about 1.3-1.0 million years ago (Nakano et al., 2001-). Ariake-yama and Hirami-yama form the high points of Tengu and Hira-yama volcanoes, respectively. The northern part of this area contains the 1.6-1.3 million year Kitamitoge volcanic rocks.

Shiitokoro
Shiitokoro-yama, an andesitic-to-dacitic lava dome and lava flow, was active about 1.4 million years ago (Nakano et al., 2001-).

Kumaneshiri
Kumaneshiri volcano consists of two andesitic-to-dacitic stratovolcanoes, Nishi-Kumaneshiri-dake and Kumaneshiri-dake, that were active about 1.3 million years ago (Nakano et al., 2001-).

Tokachi-Mitsumata
Tokachi-Mitsumata, a rhyolitic caldera that was the source of the Muka and Meto pyroclastic flows, was active about 0.6-0.3 million years ago (Nakano et al., 2001-). Ishii et al. (2008) listed dates of around 1 million years ago for formation of the Tokachi-Mitsumata caldera.

Birao
The Birao volcano group consists of Birao-yama and Sattomonai andesitic-to-rhyolotic stratovolcanoes. Birao volcano was active about 0.5-0.3 million years ago and Sattomonai volcano about 0.1 million years ago (Nakano et al, 2001-).

Samakkenupuri
Samakkenupuri volcano volcano consists of the andesitic Samakkenupuri-yama and Shibetsu-dake stratovolcanoes that were active about 1.1-0.8 million years ago (Nakano et al., 2001-).

Musa
The andesitic-to-dacitic Musa-dake volcano was active about 0.9-0.5 million years ago (Nakano et al., 2001-).

Shari
The andesitic-to-dacitic Shari-dake volcano was active about 0.3-0.25 million years ago (Nakano et al., 2001-).

Unabetsu
The basaltic-to-andesitic Unabetsu-dake stratovolcano was active about 0.9-0.5 million years ago (Nakano et al., 2001-).

Onnebetsu
Onnebetsu volcano was active about 0.4-0.2 million years ago and Chinishibetsu volcano about 0.2-0.1 million years ago (Nakano et al., 2001-).

Shiretoko
Shiretoko volcano, the NE-most in Hokkaido, was active about 0.6-0.2 million years ago (Nakano et al., 2001-). The andesitic Shiretoko-dake volcano lies at the tip of the Shiretoko Peninsula.

Urbich Caldera
Kuril Islands
The 6-km-wide Urbich caldera was formed during a Pleistocene interglacial period. A fresh-water caldera lake is present. No activity has occurred during the Holocene (Gorshkov ,1970). Urbich caldera (also known as Urumombetsu caldera partially overlies Rokko caldera.

Tsirk
Kuril Islands
The 6-km-wide Tsirk caldera formed during the Pleistocene. The caldera floor contains a hot lake (Gorshkov 1970).

Vetrovoi Isthmus Caldera
Kuril Islands
The low-lying Vetrovoi Isthmus is cut by a 6-7 km wide caldera formed during a Pleistocene submarine eruption. The caldera contains a 1-km-wide explosion crater with a small cone on its margin (Gorshkov 1970).

Petr Shmidt Ridge

Antipin

Gora Desantnaya

Brontona Island
Pleistocene according to Gorshkov (1970) map.

Ikanmikot

Kuntomintar
Kuntomintar is a Pleistocene andesitic stratovolcano that occupies the southern end of Shiashkotan Island in the central Kuriles. A central cone fills a 4-4.5 km caldera, whose rim is visible on the NE side. A second caldera on the west side is breached to the west. An Ainu village that reportedly was destroyed by an eruption in 1872 was later found to be located near Sinarka volcano (Gorshkov, 1970). The only known postglacial activity of Kuntomintar is continuous solfataric activity that originates near the east wall of the inner caldera and a nearby hot sulfur spring.

Shestakov

Avos' Rocks

Makanru Island
Mapped as Pleistocene (Gorshkov 1970).

Kamchatka Peninsula
A group of cinder cones near the Pacific Coast of Kamchatka NE of Shish volcano was mapped by Luchitsky (1974) as mid- to late-Pleistocene, but may in part be of Holocene age (Erlich 1985, pers. comm.). However, lacking any other evidence, and without evidence of young cones in satellite imagery, this is not included in the Holocene volcano list.

Vysokii
Kamchatka Peninsula
Vysokii and an unnamed volcano to the north are Pliocene stratovolcanoes with Pleistocene lava domes on or near their flanks (Masurenkov 1980).

Tumanniy
Kamchatka Peninsula
Tumanniy is a Pliocene-Pleistocene shield-like volcano with flank lava domes (Masurenkov 1980).

Ded i Baba
Ded i Baba (Ded and Baba) is an early Pleistocene shield-like volcano SW of Koshelev volcano; an unnamed mid-Pleistocene volcano with a small caldera breached to the east lies between these two volcanoes (Masurenkov 1980).

Tretya Rechka
Tretya Rechka is an early Pleistocene shield-like volcano with a small caldera open to the SE (Masurenkov 1980).

Koshegochek
Koshegochek is a Pliocene to lower Pleistocene shield-like volcano north of the Pauzhetka depression (Masurenkov 1980).

Sredniy Koshegochek
Lower Pleistocene shield-like volcano (Masurenkov 1980).

Unnamed upper Pleistocene shield volcano (Masurenkov 1980).

Leviy Koshegochek
Pliocene to lower Pleistocene shield-like volcano on north end of Golygin Ridge (Masurenkov 1980).

Kuzheten
Mid-Pleistocene shield-like volcano (Masurenkov 1980).

Kuzanek
Pliocene to lower Pleistocene shield-like volcano (Masurenkov 1980).

Lower Pleistocene shield-like volcano (Masurenkov 1980).

Igolki
Igolki and Bol'shiye Igolki are two lower to mid-Pleistocene shield-like volcanoes (Masurenkov 1980).

Skalistiy
Pliocene to lower Pleistocene shield-like volcano (Masurenkov 1980).

Perevalny
Perevalny is a small upper-Pleistocene shield volcano NNE of Khodutka volcano; an unnamed Pleistocene stratovolcano is located immediately NE of Perevalny (Masurenkov 1980).

Krugliy
Upper Pleistocene shield volcano (Masurenkov 1980).

Savan
Savan is a Pliocene to lower Pleistocene shield volcano (Masurenkov 1980).

Malaya Ipelka
Malaya Ipelka is an isolated mid to late-Pleistocene volcanic massif rising above the SW coastal lowlands north of the Opala River (Masurenkov 1980).

Kamen
Late-Pleistocene conical basaltic volcano (Masurenkov 1980).

Ploskiy
The lower-Pleistocene conical basaltic volcano Ploskiy is located west of Asacha volcano north of a large group of late-Pleistocene to Holocene pyroclastic cones (Masurenkov 1980).

Vostochnaya Khodutka
Two lower to mid-Pleistocene shield-like volcanoes (Masurenkov 1980).

Zheltiy
Small upper Pleistocene conical basaltic volcano (Masurenkov 1980).

Tolmachev
Tolmacheva and Utes are conical basaltic volcanoes of late-Pleistocene age (Masurenkov 1980).

Shemodogan
Shemedogan is a Pleistocene shield-like volcano west of the Bolshe-Bannaye ring structure (Luchitsky 1974).

Khalzan-Shapochka
Pleistocene shield-like volcano (Erlich 1985, pers. comm.).

Udochka
Udochka is a mid-Pleistocene shield-like volcano SW of Opala (Masurenkov 1980).

Bolshaya Ipelka
Bolshaya Ipelka is a massive eroded lower Pleistocene shield-like volcano that covers a 32 x 42 km area west of the main volcanic zone of southern Kamchatka. A Holocene cinder cone on the SE flank is listed separately in this compilation.

Aak
Aak, Arik, and Pinachevsky are Pleistocene volcanoes along a ridge trending NW from Koryaksky volcano. Abnormal shallow earthquakes occurred in August 1966 (Gorel'chik 1969).

Kupol
Kupol is a Pleistocene basaltic-andesite stratovolcano (Luchitsky 1974).

Kitkhoysky
Two Pleistocene shield-like volcanoes are located NW of Kupol and SW of Vershkinsky volcanoes (Erlich 1985, pers. comm.). Satellite imagery in Google Earth appears to show a 6-km-diameter caldera open to the N with a later cone or dome complex on the eastern side.

Vershinsky

Kurgannaya

Kavychinsky

Baraniy

Zhupanovskiye Vostriyaky
Large Pleistocene stratovolcano north of Zhupanova River

Ditmara
Ditmara is a broad, low stratovolcano SE of Akademia Nauk caldera.

Krainy

Razlaty

Skalistiy

Pik

Vodorazdelny

Pribrezhny
Pleistocene stratovolcanoes SE of Maly Semiachik

Unnamed Pleistocene volcano west of Boshoi Semiachik

Unana
Unana stratovolcano is of Pleistocene age; hot springs on the volcano are related to tectonic faults (Erlich 1985, pers. comm.).

Adamozhets
Pleistocene (Erlich 1985, pers. comm.)

Bogachensky
Pleistocene shield-like volcano north of Kolkhozhny volcano (Erlich 1985, pers. comm.).

Piip
Pleistocene shield-like volcano (Erlich 1985, pers. comm.).

Konechnaya
Mid to upper Pleistocene shield-like volcano (Luchitsky 1974).

Konradi
Vlasov (1967) notes postglacial activity of Konradi; later work indicates it is of Pleistocene age (Erlich 1985, pers. comm.).

Tumrok
Mid to upper Pleistocene shield-like volcano (Luchitsky 1974).

Uspensky
Mid to upper Pleistocene (Luchitsky 1974).

Shish
Mid to upper Pleistocene (Luchitsky 1974).

Iult
Iult is a large1857-m-high mid- to late-Pleistocene stratovolcano located north of Konradi volcano and NNW of the Gamchen volcanic complex. Lava domes located on the lower northern and southern flanks of Iult (also spelled Iul't) were assigned a Holocene age by Luchitsky (1974), but Andreev et al. (1988) mapped them as late-Pleistocene.

Nikolka
Pleistocene (Luchitsky 1974)

Sokol
Mid to upper Pleistocene stratovolcano north of Konradi volcano (Luchitsky 1974).

Zarechny
Zarechny is a low, forested volcano constructed in the lake-filled lowlands between Kliuchevskoi and Shiveluch volcanoes, and immediately S of Kharchinsky volcano. The 760-m-high edifice contains two nested calderas, both breached widely to the SE. The larger 4.5 x 3.7 km wide caldera is filled by an uneroded cone truncated by a 3.2 x 1.8 km wide caldera. Both horseshoe-shaped calderas resemble those produced by edifice failure, but deposits related to their origin are buried beneath younger Holocene deposits in the Kamchatka River valley. Zarechny was at one point considered to be of Holocene age (Erlich, 1986), but more recent tephrochronology has shown that the older edifice precedes formation of 23,000-24,000 year old glacial moraines, and that the younger inner edifice ceased activity during the late Pleistocene (Volynets et al., 1999).

Kharchinsky
Kharchinsky is a Pleistocene volcano immediately north of Zarechny volcano (Luchitsky, 1974) in the lowlands north of the Kamchatka River. The magnesian basaltic volcano rises 1400 m above the surrounding plains. It was constructed during the late Pleistocene and predates glacial moraines dated at 23,000-24,000 years ago. Faulting and edifice failures have deeply affected the edifice, and debris-avalanche fans are found at its base.

A group of basaltic cinder cones is located north of Kharchinsky volcano in the lowlands SW of Shiveluch volcano. The cinder cones and lava flows cover a broad area north of Kharchinsky and form a peninsula extending into Lake Kharchinsky. The cones are part of the arcuate Kharchinsky regional zone of more than 100 cinder cones, lava cones, tuyas, and explosion craters that extends across both Kharchinsky and Zarechny volcanoes and were formed during a later volcanic cycle unrelated to Kharchinsky (Erlich 1985, pers. comm.). The cinder cones initially were considered to be of late-Pleistocene to Holocene age (Luchitsky, 1974), but later tephrochronological studies have shown them to be of latest Pleistocene age (Volynets et al., 1999).

Lauchachan
Small late-Pleistocene Icelandic-type basaltic shield volcano SW of Ichinsky volcano (Ogorodov et al. 1972). The locations of many Sredinny Range volcanoes are only approximate from the ONC 1:1,000,000 scale maps and sketch maps in Ogorodov et al. 1972.

Prodolny
Prodolny and Lauchan are adjacent Pleistocene Icelandic-type shield volcanoes SW of Ichinsky volcano (Erlich 1985, pers. comm.).

Kobalan
Pleistocene basaltic stratovolcano, SW of Ichinsky volcano (Ogorodov et al. 1972).

Quaternary shield volcano west of Ichinsky volcano (Erlich 1985, pers. comm.).

A group of Pleistocene lava domes is located about 20 km ENE of Sheveluch volcano (Luchitsky, 1974).

Lyzyk
The small isolated Lyzyk volcano is probably of late-Pleistocene age (Erlich 1985, pers. comm.).

Uchkoren
Uchkoren is a small Pleistocene volcano (Erlich 1985, pers. comm.).

Nachikinsky

Khailyulya
Small Pleistocene volcano (Erlich 1985, pers. comm.).

Tynua
Two Pleistocene Icelandic shield volcanoes (Ogorodov et al. 1972).

Etopan
Late-Pleistocene Icelandic-type shield volcano (Ogorodov et al. 1972).

Kimitina
Pleistocene basaltic stratovolcano (Ogorodov et al. 1972).

Pleistocene (Erlich 1985, pers. comm.).

Ochchamo
Lower-Pleistocene shield volcano east of Ichinsky volcano (Erlich 1985, pers. comm.).

Bolshoy Kozyrevsky
Lower-Pleistocene shield volcano (Erlich 1985, pers. comm.).

Bolshaya Romanovka
Lower-Pleistocene shield volcano (Erlich 1985, pers. comm.).

Group of three Pleistocene stratovolcanoes (Erlich 1985, pers. comm.).

Bongabti
Lower-Pleistocene Icelandic-type shield volcano (Ogorodov et al. 1972).

Nosichan
Late-Pleistocene Icelandic shield volcano (Ogorodov et al. 1972).

Buduli
Late-Pleistocene Icelandic-type shield volcano (Ogorodov et al. 1972).

Kopkan
Late-Pleistocene Icelandic-type shield volcano; the Krugelenky shield to the NE along the regional NE-SW trend is listed with Kapkan volcano (Erlich 1985, pers. comm.).

Yanpat
Yanpat and Vetrovoy volcano to the north are late-Pleistocene Icelandic-type shield volcanoes (Ogorodov et al. 1972).

Chavycha
Chavycha and Olka volcano to the north are mid to late-Pleistocene Icelandic-type shield volcanoes (Ogorodov et al. 1972).

Malaya Ketepana
Malaya Ketepana is one of several large shield volcanoes along the western margin of the Sredinny Range. Smaller Icelandic-type shield volcanoes are located on the south flank and NE of Malaya Ketepana.

Bolshoy Ketepana
Bolshoy Ketepana is a large isolated lower-Pleistocene shield volcano on the west side of the Sredinny Range (Ogorodov et al. 1972).

Icelandic-type Pleistocene shield volcano (Erlich 1985, pers. comm.).

Ovalny
Mid to late-Pleistocene shield volcano (Ogorodov et al. 1972).

Tigilsky
The lower to mid-Pleistocene Tigilsky shield volcano (Ogorodov et al. 1972) appears to have a 2-km-wide crater just SE of the summit. An area on the W flank was previously listed as an Unnamed Holocene basaltic shield volcano. The morphology as observed in satellite imagery suggests that the "shield" is simply an erosional feature along a volcanic ridge of the larger edifice.

Perevalovyi
Mid-Pleistocene shield volcano with a summit caldera (Ogorodov et al. 1972).

Maly Alney
The mid to late-Pleistocene basaltic stratovolcanoes of Maly Alney and Polovinny are located SE of Alney volcano (Ogorodov et al. 1972).

Maly Chekchebonay
Mid-Pleistocene shield volcano with Hawaiian-type summit caldera (Ogorodov et al. 1972; Erlich 1986).

Bolshoy Chekchebonay
Lower-Pleistocene shield volcano with Hawaiian-type summit caldera (Ogorodov et al. 1972).

Kireunsky
Late-Pleistocene Icelandic-type shield volcano (Ogorodov et al. 1972).

Dvukhyurtochny

Group of mid-Pleistocene extrusive lava domes (Erlich 1985, pers. comm.).

Kalgauch
Late-Pleistocene basaltic stratovolcano (Ogorodov et al. 1972).

Kunkhilok
Late-Pleistocene basaltic stratovolcano east of the Sredinny Range crest (Ogorodov et al. 1972).

Shlen
Shlen is a large mid-Pleistocene shield volcano west of the main Sredinny Range (Ogorodov et al. 1972).

Pirozhnikova
Late-Pleistocene basaltic stratovolcano (Ogorodov et al. 1972).

Kamenisty
Late-Pleistocene basaltic stratovolcano (Ogorodov et al. 1972).

Tekletunup
Tekletunup is a large eroded Pliocene to lower-Pleistocene shield volcano (Ogorodov et al. 1972).

Ulvaney
Late-Pleistocene shield volcano (Ogorodov et al. 1972).

Mutny

Khuvkhoitun
The late-Pleistocene complex stratovolcano Khuvkhoitun forms the highest peak of the northern Sredinny Range. Two small late-Pleistocene shield volcanoes are located immediately to the NE (Ogorodov et al. 1972).

Keveney
Keveney is a late-Pleistocene Icelandic-type shield volcano (Ogorodov et al. 1972).

Langtutkin
Langtutkin is a late-Pleistocene Icelandic-type shield volcano east of the crest of the Sredinny Range (Ogorodov et al. 1972).

Kikhiikhylkhangei
Legends of eruptions are reported from Kikhiikhylkhangei volcano (Krijanovsky 1934), but this volcano does not appear in other lists of Quaternary Kamchatka volcanoes (Vlasov, IAVCEI 1973). The location given is NE of the northernmost Holocene volcano in the Sredinny Range and volcanoes in this region are of middle to lower Pleistocene age (Erlich 1984, pers. comm.).

Anjuisky
Russia (northeastern)
The Anjuisky (Anyuy) volcano group consists of fissure vents and small pyroclastic cones, the largest of which is 120-m high and is capped by a 300-m-wide crater. The initial fissure eruptions produced trachybasaltic lava flows 15-17 km long that covered an area of 100 km2. The most recent eruptions were considered by the Catalog of Active Volcanoes of the World (Vlodavetz and Piip, 1959) to have occurred between about 1300 and 1700 CE from Aniusk (Monni) cone, based on morphological evidence. Later work (Ignatiev, 1994) showed that Monni volcano was partially destroyed by glaciers and phreatic explosions produced by glacial meltwater flowing into the vent. Lava flows from Maly Anyuy volcano flowed onto glacial ice, and explosions induced by glacial meltwater destroyed the cone. The Monni lava flows dammed up drainages, forming lakes. During an early Holocene period of warming, large creeks overflowed from these lakes and deposited fluvial materials. The cone and lava flow are located between the Maly Anyuy and Bolshoy Anyuy rivers, about 75 km SSE of the community of Keperveyem.

Balagan-Tas
Russia (northeastern)
Balagan-Tas is a cinder cone constructed along a fault on the SW flank of the Momskiy Mountains in the NE part of Russia's Sakha Republic. A poorly preserved crater fed subalkaline basaltic lava flows that covered an area of 4-5 km2. A Potassium-Argon date of 0.3 million years was obtained (Prokopiev, 2007 pers. comm.).

Khamar-Daban
Russia (southeastern)

Dgida Basin
Russia (southeastern)
The Dgida Basin volcanic field, also known as the Dzhida Basin, is located south of the SW tip of Lake Baikal, near the border with Mongolia. One of a series of approximately E-W-trending depressions, the Dgida Basin contains Quaternary lava flows and cinder cones ranging from 55 to 240 m in height. At least two stages of volcanism are present, the first of which includes lava flows overlying the 20 m terrace of the Dgida, Darkhintuy, and Khammey rivers. In the Darkhintuy valley the lava flows are overlain by gravels, which are in turn overlaid by lava flows from the Bartoy valley. Earlier Pleistocene-to-Holocene estimates of the age of the Dgida Basin volcanism (summarized in Whitford Stark, 1987) were modified by later age-dating by Rasskazov et al. (1996), who indicated that the final stage of activity in the basin took place during the early to mid-Pleistocene.

Khulugayshi
Russia (southeastern)
Explosion crater
Tuffs from diatreme or explosion vent overlie Quaternary gravels (Whitford-Stark 1987).

Mongolia
Two upper Pleistocene volcanoes (IAVCEI 1973).

Khubsugal Region
Mongolia
Basalts dated Pliocene to Quaternary (Whitford-Stark 1987), includes basalts scattered NW and SE of above location.

Ika-Togo-Ula
Mongolia

Orkhon Gol
Basalts dated at 6.4 to 1.5 million years ago (Whitford-Stark 1987).

Tabun Urtu-Ula

Khutza-Ula
Two Pliocene-lower Pleistocene volcanoes (IAVCEI 1973).

Group of 3 Pliocene-lower Pleistocene volcanoes (IAVCEI).

Group of five volcanoes-Pliocene-lower Pleistocene (IAVCEI 1973).

Group of 5 cone-shaped volcanoes (IAVCEI 1973).

Durbulzhi-Ula
Pliocene-lower Pleistocene (IAVCEI 1973).

Ubur-Khangay
Group of six cone-shaped volcanoes (IAVCEI 1963).

China (western)
A volcanic field in NE Tibet contains a number of late-Cenozoic volcanoes (Tong et al., 1988). Several Hawaiian-style volcanoes are present in this area. Bamaoqiongzong covers an area of 300 km2 and contains a perfectly preserved edifice NE of the summit and a lava flow that overlies Quaternary lake deposits (Whitford-Stark, 1987). The Bamaoqiongzong area contains peralkaline phonolitic and foiditic rocks. Yongbohu contains five dacitic, trachyandesitic and andesitic vents. Qiangbaqian covers a broad area along the southern border of the Kunlun mountain range. Wei et al. (2003) did not note Holocene volcanoes in this region. A cone in the Kekexili caldera, once thought to be observed in eruption on a satellite photo in 1973, is now considered not to have been historically active (Kidd 1990, pers. comm.).

China (western)
Quaternary volcano (IAVCEI 1973)

China (eastern)
Quaternary basalt (Whitford-Stark 1987).

Longhai
China (eastern)
Longhai is a late-Cenozoic volcano (Tong et al. 1988) at the south end of the Zhemin Volcano Group of Chen (1986).

Jianghui Group
China (eastern)
The Jianghui Volcano Group consists of remnants of about 20 basaltic hills. Comparatively well-preserved craters exist along the eastern shore of Nushanhu and the western shore of Chaohu. The basalt is of early Quaternary age (Chen 1986; Whitford-Stark 1987, pers. comm.).

Nushan
Truncated cone of Pliocene-lower Pleistocene age (IAVCEI).

Yichuan
Late-Cenozoic volcano (Tong et al. 1988).

Tangy'n
Late-Cenozoic volcano; name appears as "Tangy n" in Tong et al. (1988).

Huixian
Late-Cenozoic volcano (Tong et al. 1988).

Heibei Plain
Late-Cenozoic volcano (Tong et al. 1988).

Late-Cenozoic "buried volcano" in the Hebei Plain (Tong et al. 1988).

Taihangshanlu
Whitford-Stark (1987) notes a report of probably Oligocene-aged basalts in the central Taihang Range. Tong et al. (1988) map a late-Cenozoic volcano at this location.

Late-Cenozoic "buried volcano" in Hebei Plain (Tong et al. 1988).

IAVCEI lists a volcano in this location. Tapponnier and Molnar (1977) show two flows at 40.25 N 113.52 E which may be the same area (Whitford-Stark 1987).

Datong-Fengzen
The Datong-Fengzhen volcano group, also known as Ta-T'ung or Fanjiatun, is located at the intersection of two regional fault zones. The volcanic field contains about 80 volcanic vents, including cinder cones and small lava domes. The central Datong group contains 12 cones. An historical eruption reported during the 5th century (Chen 1986) has been shown to have originated from spontaneous combustion of a Jurassic coal seam (Zhang 1989, pers. comm.). The 13 youngest cones of the volcanic field have been Potassium-Argon dated at 0.34-0.37 million years.

Includes 2 volcanoes (IAVCEI 1973).

Includes 3 volcanoes.

Chifeng

Dalainuoer
Tapponnier and Molnar (1977) document from satellite photographs a large volcanic field with fresh features suggesting possible eruptions within historical times. Hang (1989 pers. comm.) indicates that extensive dating by Yang indicates the youngest eruptions were of late Pleistocene age.

Nuomin
The Nuomin volcanic field, identified as Shatu in Ogara (1969) and Whiford-Stark (1987), is dominated by monogenetic cones and lava flows that cover about 600 km2 (Zhao and others, 2014). K-Ar dating by Fan and others (2012, cited in Zhao and others, 2014) indicated eruptions between 2.3 and 0.13 Ma. The most recent activity was at the Sifang Mountin, which is the southern-most cone of the group and contains a small lake in the summit crater.

Jianshan
Jianshan volcano (at the Jianshan Farm) is located NW of the Wudalianchi volcanic field. Zhao and others (2014) reported that this isolated monogenetic cinder cone was K?Ar dated at 0.12 ± 0.02 Ma.

Erkeshan
Two adjacent volcanic cones are located just NE of the city of Kedong in the Heilongjiang Province of far northeastern of China. The larger eastern cone is about 700 m in diameter, and the smaller western one is 600 m. A third circular feature about 200 m in diameter forms a very low (12 m high) hill about 1 km NW of the western cone. Zhao and others (2014) reported a date of 0.43 +/- 0.01 Ma for the north cone, and noted that Liu and others (2001) had dated the east cone at 0.563 +/- 0.133 Ma.

Dunhua
Dunhua was described by Whitford-Stark (1987) as being composed of flows of two or three different ages.

Yitong Group

Fanjiatung Group

Kuandian

Kilchu-Myongch'on
Korea

Koksan-Singye
Korea
Listed as probably active in last 2000 years by IAVCEI, but Whitford-Stark lists as Pleistocene and Tomita (1967) states there has been no Holocene volcanism on the Korean Peninsula.

Sergief
Aleutian Islands
Sergief is a small stratovolcano on SW Atka Island whose age is poorly known. The SW part of the island is older and less topographically rugged than the NE part of the island. It was tentatively listed as a young volcano in the Post-Miocene Volcanoes of the World catalog of the International Association of Volcanology and Chemistry of the Earth's Interior (1973), but the age of its latest eruption is not precisely known.

Adagdak
Aleutian Islands
Mount Adagdak, at the NE tip of Adak Island, lies across Andrew Lagoon from Mount Moffett volcano and about 15 km NNE of Adak, the largest town of the Aleutians. Adagdak consists of a small stratovolcano capping an older shield volcano exposed on the southern side of the complex. An andesitic lava dome fills the summit crater. A late-stage basaltic lava dome was constructed on the SE flank, and a phreatic vent is located on the western flank of the shield volcano. The most recent eruptions have been considered to be Holocene (Marsh, in Wood and Kienle 1990) or Pleistocene (Motyka et al. 1993, Nye et al. 1998). Three stages of volcanism were mapped by Bratten, the youngest of which was a lava dome dated at about 0.21 million years (AVO, 2005-). The older Andrew Bay volcano, located north of Andrew Lagoon between Adagdak and Moffett volcanoes, is preserved only in erosional remnants. Andrew Bay Hot Springs lie along the coast west of Mount Adagdak, and the northern part of Adak Island has been investigated for geothermal power potential.

Table Top
Aleutian Islands
Table Top and Wide Bay cinder cones, at the NE tip of the triangular NW extension of Unalaska Island across the bay from the town of Dutch Harbor, blanket or fill late-Pleistocene topography. Both 792-m-high Table Top and the 640-m-high Wide Bay cones were considered to be Holocene in age, with the Wide Bay cone being among the youngest in a SW-NE-trending volcanic belt that passes through Makushin volcano (Miller et al., 1998), however, a later 40Ar/39Ar age of 68+/-14 ka was obtained from Table Top (AVO, 2005-). Table Top Mountain cone has an associated lava apron and was considered to represent a magmatic system separate from that of Makushin volcano and Wide Bay cone (Nye, pers. comm. 2008).

Wide Bay
Wide Bay and Table Top cinder cones, at the NE tip of the triangular NW extension of Unalaska Island across the bay from the town of Dutch Harbor, blanket or fill late-Pleistocene topography. Both 792-m-high Table Top and the 640-m-high Wide Bay cones were considered to be Holocene in age, with the Wide Bay cone being among the youngest in a SW-NE-trending volcanic belt that passes through Makushin volcano (Miller et al., 1998), however, a later 40Ar/39Ar age of 19+/-15 ka was obtained from Table Top (Nye, 2008 pers. comm.). Lowermost flows at the base of the cone are glacially striated although the cone remains well shaped with the summit vent depression preserved. Wide Bay was considered to represent a magmatic system separate from that of Makushin volcano and Table Top cone (Nye, pers. comm. 2008).

Gilbert
Mount Gilbert is deeply eroded and an area of former solfataric activity appears to have been glaciated. Solfataric activity had ceased between 1942 and 1945 (Byers and Barth 1953).

Trader Mountain
Alaska Peninsula
Trader Mountain is a small dacitic stratocone-like feature with an extrusive dome; lava flows dip away from the center in all directions (Chris Nye, oral commun., 2007). Wilson and others (1995) alternatively described Trader Mountain as a hypabyssal dacite plug, and report a potassium-argon age of 0.98+/- 0.05 Ma (F.H. Wilson and Nora Shew, unpub. data, 1988).

Stepovak Bay 1
Alaska Peninsula
The southwesternmost of a chain of five volcanoes north of Stepovak Bay is of Pleistocene age. K-Ar dates of about 0.53 and 0.4 million years were obtained (Wilson, 1989).

Blue Mountain
Alaska Peninsula
The Blue Mountain lava dome cluster immediately west of Upper Ugashik Lake consists of 13 dacitic lava domes. An Ar/Ar date of about 632,000 years was obtained from the highest dome.

Gertrude Creek
An ice-scoured basaltic scoria cone and associated lava-flow apron lies at Getrude Creek about 5 km NE of Becharof Lake. The cone was constructed near the trace of the Bruin Bay fault and was Argon-Argon dated at about 500,000 years BP (Hildreth et al., 2003).

Devils Desk
Devils Desk, which rises 450 m above the top of Hook Glacier to its west, is the eroded neck of a former stratovolcano, most of which has been removed by extensive erosion. Three radial dikes exposed as ridges extend from the volcano toward the east. Devils Desk lies at the NE end of a glacier-mantled range containing small closely spaced volcanic centers that extends from Snowy Mountain, NE of Mount Katmai. The age of Devils Desk volcano is not known precisely. Although it was included in a list of probable Holocene volcanoes (Smith et al., 1978), extensive glacial dissection suggests it could be of Pleistocene age (Motyka et al., 1993), and Hildreth et al. (2003) obtained a Potassium-Argon date of about 245,000 years from a block on the SW face, similar to the age of one of the nearby rear-arc Savonoski cones.

Savonovski River Cluster
A group of small Pleistocene stratovolcanoes and a scoria cone lies behind the volcanic front near the headwaters of the Savonovski River, NW of the Denison to Devils Creek alignment of volcanoes. Dated ages range from about 88,000 to 390,000 years (Hildreth et al., 2003).

Double Glacier
Alaska (southwestern)
Double Glacier volcano is a Pleistocene lava dome complex forming a nunatak in Double Glacier. Potassium-Argon dates range from 627 to 887 thousand years ago (Reed et al. 1992). Nearby Double Peak, 5 km to the north, was once thought to be a volcano (Coats 1950, IAVCEI 1973), but reconnaissance mapping indicates the peak probably consists of Jurassic plutonic rocks (Reed et al. 1992).

Nunivak Island
Alaska (western)
Nunivak Island contains about 60 cinder cones and four maars; the surface of the island is dominated by thin pahoehoe lava flows that form a carapace over Cretaceous sedimentary rocks. The 110-km-wide permafrost-covered island lies about 30 km off the coast of SW Alaska. The widespread lava flows originate from small shield volcanoes and cover much of the island, which is dotted throughout by cinder cones and other vents. Two of the maars have about 200 m of relief, with floors near sea level. Eruptions occurred during five broad periods of activity that began 6.1 million years ago and continued until about 150 ka. The bulk of the >427 km3 volcanic field was formed during two Pleistocene eruptive periods that ended about 300,000 years ago. The most recent eruptions produced a series of alkalic basalt lava flows and ash deposits from cinder cones and maars along an E-W zone in the southern part of the island.

Kookooligit Mountains
Alaska (western)
The Kookooligit Mountains are a 30 x 40 km wide shield volcano of Pleistocene-to-Holocene age in north-central St. Lawrence Island. The basaltic shield is composed of massive columnar-jointed lava flows that are overlain by more than 100 small cones (20-60 m high). Most of the cones are aligned E-W along the crest of the elongated shield volcano.

St. George
Alaska (western)
St. George Island is comprised of Tertiary to late-Pleistocene cones and lava flows (Lee-Wong, in Wood and Kienle 1990). An eruption was reported NE of St. George in 1815 but "in spite of these assertations any present volcanic activity must be regarded as doubtful" (Barth 1956).

Otter Island
Late Pleistocene (IAVCEI).

Walrus Island
Late Pleistocene (IAVCEI).

Togiak Valley
The Togiak volcanics are a late-Pleistocene sequence of thin lava flows that includes the subglacially formed Togiak Tuya (Wood and Kienle 1990).

Ingrichuak Hills
The Ingrichuak Hills consist of at least five low lava shields of probably Quaternary age (Moll-Stalcup, in Wood and Kienle 1990).

Selawik Hills
Includes six vents and other scattered lava fields to south of Selawik Hills (IAVCEI) of Tertiary to Pleistocene age.

Espenberg
One of the northernmost areas of Quaternary volcanism in North America, the Espenberg volcanic field, is located at the northern tip of the Seward Peninsula just south of the Arctic Circle. The five maars, the largest known on Earth, were erupted through thick permafrost during the late Pleistocene. They were at one time considered to have been active into the Holocene (from about 120,000 to about 7000 years ago), but later radiocarbon dating indicated that the youngest maar, Devil Mountain, erupted about 17,500 years ago (Begét et al., 1996). The compound Devil Mountain maar, consisting of two intersecting craters, is 8 x 6 km wide, and North and South Killeak maars are 4 and 5 km wide, respectively. Whitefish maar is 4.3 km wide. The maars were excavated 100-300 m below the ground surface, with lake surfaces 60-80 m below the surrounding topography. The late-Pleistocene basaltic field also contains five older small shield-like volcanoes.

Sanford
Alaska (eastern)
Massive dissected Mount Sanford shield volcano is one of the highest Quaternary volcanoes in the United States. The glacier-covered andesitic volcano towers above the Copper River and has a broad, bulbous top that is surrounded by massive, glacially excavated cirques, most prominent on the SW and SE sides of the summit. The upper part of this little-studied, ice-covered volcano is possibly of Holocene age (Richter, in Wood and Kienle, 1990) and developed on a base of three coalescing andesitic shield volcanoes south, NW and NNW of the summit that began to form about 900,000 years ago. A massive mid-Pleistocene rhyolitic lava flow from a NE-flank vent traveled more than 18 km to the NE. Basaltic lava flows that were erupted from a NE-flank rift zone about 320,000 years ago mark the latest radiometrically dated activity.

Gordon
Alaska (eastern)
Mount Gordon is the most prominent of a group of Pleistocene and Holocene cinder cones in the northern Wrangell Mountains SE of Tanada volcano. Most are less than 100 m high, but Mount Gordon is a composite basaltic cinder-lava cone 5 km in diameter and 625 m high. Many of the cones retain their original constructional forms (Richter, in Wood and Kienle, 1990). Construction of the largely ice-covered Gordon was preceded by the effusion of basaltic lava flows, and airfall deposits from the cone blanket the area; the precise age is not known.

Jumbo Dome
Alaska (eastern)
Jumbo Dome is a large cylindrical plug of hornblende andesite 1.6 km long, 1.3 km wide, and 500 m high which intrudes the Devonian Keevy Peak Formation basement and overlying Tertiary Suntrana Formation (AVO, 2005-). Ar/Ar dating by Athey et al. (2006) yielded an age for Jumbo Dome of 1.026 +/- 0.057 Ma.

Prindle
Prindle volcano is a small isolated basaltic cinder cone and lava flow in an area of metamorphic and granitic terrain. The cone formed sometime between the early Pleistocene and the about 1900 years before present White River ash that overlies the lava flow; Foster (in Wood and Kienle 1990) considered Prindle to be of Pleistocene age.

Capital
The relatively small Capital Mountain andesitic shield volcano, north of Mount Sanford, contains a 4-km-wide summit caldera apparently of non-explosive origin. Shield and intracaldera lavas and dikes are dated 1-1.1 Ma (Richter, in Wood and Kienle 1990).

Drum
The westernmost volcano of the Wrangell volcanic field, Mount Drum was formed during two cycles of activity between about 750 and 250 ka, the last of which included the emplacement of an arcuate ring of ten dacitic lava domes between 350 and 250 ka (Richter et al. 1994). The latest activity resulted in destruction of the southern half of the volcano and the formation of debris avalanches that covered a 200 km2 area during the late Pleistocene.

Tanada
Tanada Peak is an eroded remnant of an andesitic shield volcano with a former 8 x 6 km summit caldera. The 1-2 Ma old shield lavas are mostly eroded away, but younger cones are found to the north and south (Richter, in Wood and Kienle 1990).

Jarvis
Mount Jarvis, part of the eastern Wrangell volcanic field is dated at 1-2 million years ago (Richter, in Wood and Kienle 1990).

Basalt Knob
Mapped as Quaternary?; not likely present when glacial erosion formed inlet (Rossman 1959).

Skookum Creek
The Alaska Volcano Observatory describes this volcano as follows, from Miller and Richter (1994): "The Skookum Creek eruptive center is an erosionally dissected complex that may, in part, be as young as Quaternary. It consists principally of a series of rhyolite, rhyodacite, and andesite domes and their associated pyroclastic deposits, with an age of about 3.7 Ma, and an extensive sequence of relatively flat-lying andesite flows, some of which have been dated at 2.8 Ma (Lowe and others, 1982). Both the domes and the flows are intruded by a few rhyodacite and andesitic dikes that appear to originate from a rhyodacite dome near the center of the complex. Relations between the volcanic units of the complex suggest that the flat-lying flows fill a caldera that is defined by the crude arcuate alignment of the domes."

Satah Mountain
Canada
The Satah Mountain Volcanic Field on the Chilocotin-Nechako Plateau in central British Columbia consists of a N-S-trending chain of pyroclastic cones (Hickson 1990, pers. comm.). This long ridge of trachytic lava domes and flows, and basaltic and trachybasaltic pyroclastic cones, extends south from the felsic Itcha Range volcanic complex. The youngest cone is well preserved and could be of comparable age to the 7200-year-old Nazko cone 80 km NE (Charland et al., 1993). However, Ar-Ar dating of multiple cones by Kuehn et al., 2015) found that the youngest was about 1.43 Ma. Kuehn et al. (2015) also interpreted Satah as belonging to the Anahim Volcanic Belt.

Kawdy Metah
Canada
The Kawdy Metah volcanic field lies along the Kawdy Plateau north of Level Mountain and contains a group of tuyas and subglacial mounds of Pleistocene age (Hickson et al., 1994).

Dark Mountain
Canada
The Dark Mountain volcanic field in the Cassiar Mountains consists of remnants of a group of subglacial mounds now forming volcanic rock outcrops east of Dease Lake and east of the Tuya Butte and High Tuya Lake subglacial volcanic fields (Hickson et al., 1994).

Klastline Group
At least six vents on the Klastline Plateau, the largest of which is the volcanic neck of Castle Rock, are mapped as Quaternary and have produced linear ridges composed of subglacial piles of pillow lava and tuff-breccia (Souther, 1972). Rocks nearby the Stikine River volcanic field are Potassium-Argon dated from 4.6-5.4 million years ago (Hickson, in Wood and Kienle, 1990).

Hogum Range
The Hogum Range contains a group of at least 7 volcanic necks which are associated with dikes, lava flow remnants, and pyroclastic cones. Some of the cones contain striated boulders, occur in places where they would have been destroyed by Pleistocene glaciers, and are considered to be of Recent age by Lord (1948). Souther (in Wood and Kienle, 1990) indicates that the relationship of intravalley flows to the present topography suggests a Quaternary age. Recent work indicates all activity ceased during the Pleistocene (Hickson et al., 1994).

Alice Arm
Eroded volcanic outcrops of Pleistocene age are found in the Alice Arm area west and north of Tseax River Cone (Hickson et al., 1994).

Itcha Range
The Itcha Range, one of the Miocene to Pliocene felsic shield volcano complexes of the Anahim Volcanic Belt in central British Columbia, is capped by a large number of basaltic cinder cones of Pliocene to latest Pleistocene age. The highly dissected complex covers an area of 300 km2. Potassium-Argon dates on the younger pyroclastic cones and tuff rings, primarily in the eastern half of the complex, range from 2.2 to 0.8 million years ago (Ma). The youngest lavas are basanite flows in the NW and NE part of the complex. The freshest and best preserved cinder cone in the center of the shield could be much younger, perhaps as young as the 0.34 Ma - 7100 years before present Nazko cone to the east (Charland et al., 1993). The cone has not been dated and the latest volcanism is most likely of latest Pleistocene age (Hickson et al., 1994).

Quesnel Cone Group
A group of pyroclastic cones of Pliocene to Quaternary age are located near Quesnel Lake. The Abbott Creek Cone, about 6.5 km N of Quesnel Lake, was given an Ar-Ar age of 180 ka by Kuehn et al. (2015), confirming the Quaternary activity. However, another outcrop thought to be Quaternary yielded a Jurassic Ar-Ar age (Kuehn et al., 2015).

Chilcotin Group-North
The Chilcotin basalts form an extensive series of flat-lying basaltic lava flows of Miocene to Pleistocene age covering the interior of British Columbia (Mathews, 1989). The flow remnants form eroded volcanic outcrops that appear to have been erupted from now-eroded coalescing small shield volcanoes scattered throughout the intermontaine region. Most flows are 5-10 m thick, but locally are very thick (up to 200 m) where they fill palaeovalleys. In some instances thick sequences of pillows are found, in other localities they form a thin veneer under glacial drift. The Chilcotin basalts are listed here in two groups--a northern group in the Chilcotin Plateau area, and a southern group in the Thompson Plateau. Eroded volcanic outcrops of Pleistocene age of the northern Chilcotin group are found at Alixton Creek, Big Bar, Browns Lake, Crows Bar, Dog Creek, Prentice Gulch, and Thaddeus Lake (Hickson et al., 1994).

Squamish
The Squamish volcanic field contains the southernmost vents of the Garibaldi volcanic belt. Late Pleistocene eruptions formed The Castle, a dramatic strongly jointed spire above the town of Squamish formed by ice contact lava extrusion (Mathews, 1958), and Watts Point, on Howe Sound south of Squamish, formed by subglacial valley floor lava extrusion. The dacite flows at Watts Point are Potassium-Argon dated at 0.09 and 0.13 million years (Green et al., 1988).

Chilcotin Group-South
The southern part of the Miocene to Pleistocene Chicotin basalts forming an extensive series of basaltic lava flows covering much of the Thompson Plateau and Okanagan Highland in the interior of southern British Columbia are referred to as the Chilcotin Group-South. These basalts are tectonically and petrologically similar to the Chilcotin basalts to the NW, listed separately in this compilation. The Chicoltin basalts appear to have been erupted from discrete centers, no longer preserved, and form scattered outcrops of thin basaltic flows that are locally thick where they fill palaeovalleys. Five areas of Recent volcanic deposits are mapped north of Princeton and SE of Merritt (Church and McAdam, 1983). Two Potassium-Argon dates of 0.04 million years ago have been obtained on these rocks (Hickson, in Wood and Kienle, 1990), and the Chilcotin basalts are considered to be no younger than late Pleistocene (Hickson et al. 1994). Eroded volcanic outcrops of Pleistocene age in the southern Chilcotin group are found at Kelowna, Lambley Creek, Missezula Lake, Nicola (Chester), Quilchena Creek, and West Kettle River (Hickson et al., 1994).

Baldface Mountain
The Baldface Mountain Volcanic Field is part of the Anahim Volcanic Belt in central Britich Columbia, between the Itcha Range and Nazko Cone. The youngest Ar-Ar age found by Kuehn et al. (2015) was 0.91 Ma from a hawaaite flow 6 km SE of Baldface Mountain.

Tumac Mountain
USA (Washington)
Tumac Mountain cinder cone north of White Pass was mapped as Holocene (Simmons et al. 1983), however tephra studies indicated that the last eruption was 20-30,000 years before present (Schasse 1987).

Goat Rocks
USA (Washington)
The deeply eroded Goat Rocks stratovolcano was active between about 2.5 and 0.5 million years ago (Ma) (Swanson, in Wood and Kienle 1990). The andesitic volcano was constructed between about 2.5 and 0.5 Ma over older products of a major rhyolitic explosive eruption. During the late Pliocene and early Pleistocene the small Hogback Mountain shield volcano was constructed south of White Pass. About 1.0 Ma the Tieton Andesite, the earth's largest known andesitic lava flow, traveled 80 km to the east. Following extensive erosion, mid to late Pleistocene andesites were erupted onto the glaciated Cispus River valley.

Marble Mountain
USA (Washington)
Marble Mountain, an andesitic shield volcano lying SE of Mount St. Helens and north of Swift Reservoir, was last active about 0.16 million years ago (Wood and Kienle, 1990). It lies at the NW end of a chain of Quaternary volcanoes extending SE to the Colombia River.

Simcoe
The Simcoe volcanic field, of Pliocene-to-Pleistocene age, lies east and SE of Mount Adams. Small shield volcanoes and cinder cones, many erupted along N-S fissures, range in age to about 0.5 million years old.

Lava Mountain
USA (Oregon)
The Lava Mountain lava field, also known as the East lava field or Squaw Ridge lava field, is the middle of a group of three young basaltic fields located in the High Lava Plains SE of Newberry volcano. In contrast to the small fissure vents of the adjacent Devils Garden lava field, the Lava Mountain field consists of a shield volcano capped by the Lava Mountain pyroclastic cone complex that forms a prominent topographic high. Lava flowed in all directions for distances up to 6 km from the summit cone complex. The age of the lava field is not known directly, but Lava Mountain is thought to have been formed during the same eruption as nearby Four Craters lava field (only 6 km away), whose vents share alignment along the regional fault system extending from Christmas Valley NNW to Quartz Mountain. Both lava fields have similar lava chemistry and paleomagnetic directions, and the Four Craters eruption was dated based on surface exposure evidence by Mackey et al. (2012) to 13 ka.

Four Craters Lava Field
USA (Oregon)
The Four Craters Lava Field is the SE-most of a group of three basaltic lava fields SE of Newberry volcano in the High Lava Plains of central Oregon. The Four Craters Lava Field originated from four pyroclastic cones that were constructed along a roughly 4-km-long NW-SE-trending line. The NW-most and highest cone has a well-preserved crater rim. The other cones are breached to the west, SW, and south, respectively. Multiple surface exposure dates place the emplacement of the Four Craters lava field at about 13 ka (Mackey et al., 2012).

Boring Lava
USA (Oregon)
The Boring Lava volcanic field, underlying part of the city of Portland, Oregon and neighboring areas to the east and across the Columbia River in Washington, was active from the Pliocene until about the mid-Pleistocene. The volcanic field consists of at least 32 to perhaps 50 small basaltic shield volcanoes and cinder cones, with a large concentration of vents located NW of the town of Boring, Oregon. Larch Mountain shield volcano near the eastern end of the volcanic field is the highest summit at 1236 m; most cones are about 200-300 m elevation. These volcanoes lie about 100 km west of the main Cascade Range volcanoes.

Defiance
Mount Defiance, and andesitic shield volcano, lies south of the Columbia River Gorge and SW of the town of Hood River, Oregon.

Lost Lake Butte
Andesitic Lost Lake Butte shield volcano lies NW of Mount Hood volcano and overlooks Lost Lake.

Wilson
Mount Wilson shield volcano is the most prominent of a group of Pleistocene shield volcanoes between Olallie Butte and Mount Hood (Sherrod, in Wood and Kienle, 1990). Summit Butte shield volcano lies to the SW and Clear Lake Butte to the NW.

Olallie Butte
Ollalie Butte is a basaltic-andesite shield volcano that is older than about 25,000 years before present. North Pinhead cinder cone to the north is even younger, but its flows are glaciated, suggesting an age of >11,000 years (Sherrod, in Wood and Kienle 1990). Sisi Butte, another shield volcano and other cinder cones are located nearby.

Three Fingered Jack
Three Fingered Jack is a distinctive deeply eroded basaltic andesite shield volcano that forms the highest peak between Mt. Jefferson and the Three Sisters. A pyroclastic cone buttressed by radial dikes forms its sharp-ridged summit. Other Pleistocene shield volcanoes and cinder cones are found to the NW and SW, and Hogg Rock Butte near Santiam Pass is a tuya formed during subglacial eruptions. The Maxwell Butte shield volcano SW of Three Fingered Jack is less eroded, and erupted between about 80,000 and 40,000 years before present.

Black Butte
Black Butte is prominent small stratovolcano east of Cascade Range crest. Despite its youthful profile, Black Butte is older than many other Cascade Range stratovolcanoes because of its position in a rain shadow to the east. Potassium-Argon dates average around 0.45 million years ago (Taylor, 1981). A NW-SE-trending chain of Pleistocene cinder cones lie east of Black Butte, and other Pleistocene cinder cones lie to the south.

Washington
Mount Washington is an eroded Pleistocene basaltic-andesite shield volcano capped by a steep-sided central plug that is the most prominent landmark between North Sister and Three Fingered Jack volcanoes. The Cache Mountain cinder cones lie to the NE, and the Hayrick Butte tuya and the Recent cinder cone Hoodoo Butte to the NW. A series of aligned spatter cones on the NE flank along a regional fissure that extends to about 4 km from the summit erupted about 1300 years ago, but ejecta from this chain is petrographically similar to Blue Lake Crater ejecta and is considered to have erupted at the same time (Sherrod et al., 2004).

Black Crater
Black Crater is a Pleistocene basaltic-andesite shield volcano SE of Belknap volcano. Trout Creek Butte volcano lies to the SE of Black Crater, and scattered Pleistocene cinder cones lie to the NE.

Scott Mountain
Scott Mountain is a Pleistocene basaltic-andesite shield volcano lying SW of Belknap volcano.

Tumalo
The Tumalo volcanic center is the inferred source of large-volume Pleistocene ashflows such as the Desert Spring Tuff, the Bend Pumice and Tumalo Tuff, and the Shevlin Park Tuff. The area contains a large number of rhyolitic domes, such as Melvin Butte, and andesitic cinder cones, such as those in the Triangle Hill area, which are compositionally similar to the Tumalo Tuff (and correlative Bend Pumice) and Shevlin Park Tuff, respectively.

Broken Top
Broken Top is a complex dominantly basaltic-andesite stratovolcano immediately SE of South Sister volcano. It is extensively eroded by glaciers, with the summit crater breached to the SE. Intermittent eruptions of andesite, dacite, and rhyolite have produced lava flows, pyroclastic flows, and airfall tephra. A late Pleistocene or early Holocene debris avalanche traveled 7 km N (Hildreth et al., 2012). Cayuse Crater on the upper SW flank of Broken Top is considered to be related to a possible magma chamber underlying the South Sister area, and is assigned to South Sister rather than Broken Top (Fierstein et al., 2011). A radiocarbon age of 9520 +/- 100 years before present (BP) from sediment beneath Cayuse Crater scoria is considered to be suspect because of lack of pretreatment and possible contamination by younger material. The scoria overlies glacial till considered to be 11,000-12,500 or as old as 14,000 years BP (Sherrod 1995, pers. comm.).

Williamson Mountain
Williamson Mountain, the highest of a group of small Pleistocene shield volcanoes or large cinder cones SW of Mount Bachelor, is flanked by Elk Mountain to the north and Sixbit Point to the WSW. A N-S-trending chain of cinder cones lies between Elk Mountain and Sixbit Point, and Packsaddle Mountain shield volcano lies west of Sixbit Point.

Irish Mountain
Irish Mountain, a Pleistocene shield volcano SW of Williamson Mountain, was roughly estimated to be 0.25-0.73 million years (Sherrod, in Wood and Kienle, 1990). A N-S-trending chain of cinder cones cuts across Irish Mountain.

Taylor Butte
The Pleistocene Taylor Butte shield volcano lies SW of Irish Mountain. A chain of N-S-trending cinder cones lies SSW of Taylor Butte.

Cultus Mountain

Wuksi Butte-Twin Lakes
The Wuksi Butte-Twin Lakes volcanic field is a 7-km-long N-S trending chain SW of Lookout Mountain consisting of scoria cones at the north and three tuff rings up to 1 km in diameter at the south. At one time considered to be of probable Holocene age (Smith et al.1978), the chain is now thought to have last been active during the latest Pleistocene--lava flows are overlain by a well-developed soil beneath the Mazama ash, suggesting that the volcanic chain is considerably older than 6800 years before present (Scott et al., 1989).

Cupit Mary Mountain
Cupit Mary Mountain, a basaltic-andesite shield volcano west of Waldo Lake, has K-Ar dates of 0.3 and 0.68 million years (Sherrod, in Wood and Kienle, 1990).

Fuji Mountain
Fuji Mountain shield volcano SW of Waldo Lake was considered to of Pleistocene age (Sherrod, in Wood and Kienle, 1990). Mount Ray to the ENE, south of Waldo Lake is reversely polarized and older than 0.73 million years.

Maiden Peak
Maiden Peak is the highest and southernmost of a chain of Pleistocene shield volcanoes and pyroclastic cones extending from north of Odell Lake to Charlton Butte. The Twins shield volcano lies across a low saddle north of Maiden Peak, Maklak Mountain lies to the SE of Maiden Peak, and an unnamed volcano that is the site of the WIllamette Pass ski area lies immediately SW of Maiden Peak.

Red Top Mountain
Red Top Mountain and Lakeview Mountain shield volcanoes of Pleistocene age lie between Odell and Crescent Lakes.

Cowhorn Mountain
The glacially modified Cowhorn and Sawtooth Mountain shield volcanoes and adjacent cinder cones lie SW of Crescent Lake. A lava from Sawtooth Mountain, located SW of Cowhorn Mountain was K-Ar dated at 0.56 and 0.52 million years (Sherrod, in Wood and Kienle, 1990).

Cappy Mountain
Cappy Mountain is a large, dissected mid-Pleistocene stratovolcano NNE of Mt. Thielson and south of Crescent Lake with rhyodacitic lavas around its flanks.

China Hat-East Butte
China Hat and the adjacent East Butte silicic lava domes, located ESE of Newberry volcano, have K-Ar dates of 0.8 and 0.87 yr BP, respectively.

Quartz Mountain
Quartz Butte lava-dome complex, ESE of the China Hat-East Butte lava domes, have a K-Ar date of 1.1 million years.

Fort Rock Volcanic Field
A large group of tuff rings, tuff cones, and maars occupies the Fort Rock-Christmas Lake Valley basin S of Newberry volcano. The 64 x 40 km basin was occupied a Pliocene to late-Pleistocene lake, through which eruptions of basaltic magma occurred along faults cutting diagonally across the basin and adjacent highland. The volcanic field is named for Fort Rock, a spectacular wave-cut tuff ring that was breached by wave erosion. The Table Rock tuff ring and maar complex lies at the SE end of the field. Spectacular maars such as Hole-in-the-Ground and Big Hole are located near Gighway 31. Hole-in-the-Ground was formed as recently as between 13,500 and 18,000 years ago.

Diamond Peak
Diamond Peak, a basaltic-andesite shield volcano, dominates the Willamette Pass area. Capped by a pyroclastic cone, Diamond Peak probably erupted in the last 100,000 years. but is older than the last glaciation at about 11,000 years (Sherrod, in Wood and Kienle 1990). An older shield volcano, Mt. Yoran, lies to the NNE and the Diamond Rockpile and Crater Butte cinder cones lie to the south.

Thielsen
The eroded central plug of Mount Thielsen forms a prominent summit spire known as the "Lightning Rod of the Cascades." The heavily eroded volcano is Potassium-Argon dated about 0.29 million years ago (Sherrod, in Wood and Kienle 1990). Pre-Thielsen shield volcanoes lie to the east and NE and pyroclastic cones to the south and SW.

Bailey
Mount Bailey is the southernmost of a N-S chain of volcanoes west of Diamond Lake. Volcanism migrated to the south, with Mount Bailey being late Pleistocene in age, between 100,000 and 11,000 years before present (Sherrod, in Wood and Kienle 1990).

Goose Nest
Goose Nest was considered to be a Holocene andesitic shield volcano and pyroclastic cone south of Crater Lake by Sarna-Wojciki et al. (1983). Sherrod (1995 pers. comm.) noted that mapping by Willie Scott shows it to be older than 13,000 years before present.

Big Bunchgrass
The basaltic Big Bunchgrass pyroclastic cone was considered to be of Holocene age (Sarna-Wojcicki et al. 1983, Smith 1988). The age assignment of Smith was based on lack of observation of Mazama tephra at Big Bunchgrass, but Sherrod (1995 pers. comm.) has found overlying Mazama tephra, and considers Big Bunchgrass to be substantially older than Holocene based on degree of erosion.

Imagination Peak
Imagination Peak pyroclastic cone NW of Pelican Butte was considered to be of Holocene age (Sarna-Wojcicki et al. 1983, Smith 1988), but Sherrod (1995 pers. comm.) considered a Holocene age to be uncertain, based on the lack of a summit crater and possible glaciation. The sharp-topped summit without a crater is morphologically similar to Lone Peak in the southern Cascades of Washington, a tuya constructed through a glacial icesheet or glacial lake.

Sprague River Valley
The basaltic-to-dacitic Sprague River Valley volcanic field consists of small shield volcanoes, cinder cones, and about two dozen maars active from 5-1.5 million years ago (Sherrod, in Wood and Kienle, 1990). The youngest features of the volcanic field are the Saddle Mountain basaltic-andesite shield volcano and Taylor Butte, a basaltic cinder cone.

Pelican Butte
Pelican Butte, one of the largest volcanoes between Crater Lake and Mount Shasta, is a late Pleistocene andesitic shield volcano. Located slightly east of the Cascade Range crest, Pelican Butte is cut by a broad cirque on the NE side and is probably no younger than about 60,000 years before present (Smith, in Wood and Kienle 1990).

McLoughlin
Mount McLoughlin is a large basaltic-andesite lava cone containing a pyroclastic core exposed by glaciation that is capped by an armor of andesitic lava flows from summit and flank vents. The latest flows were considered by Maynard (Harris, 1988) to probably be of similar age to the young McKenzie Pass lava flows in the central Oregon Cascades, but Smith (in Wood and Kienle 1990) estimated the age of the youngest flows as about 20,000 to 30,000 years.

Brown Mountain
Brown Mountain, SE of Mount McLoughlin, is a forested basaltic-andesite shield volcano with fresh, unvegetated lava flows descending as far as the base of the volcano on three sides. The latest flows are estimated by Williams (1942) to be possibly only a few centuries old, but Smith (in Wood and Kienle 1990) brackets the age of Brown Mountain between 60,000 and 12,000 years.

Mountain Lakes
The Mountain Lakes volcanic field, located east of Brown Mountain and NW of Klamath Falls, is a Pliocene-to-Quaternary cluster of andesitic volcanic vents. The volcanic field contains Aspen Butte and LIttle Aspen Butte, the latter a shield volcano that is the southermost Quaternary volcano in Oregon (Hildreth, 2007).

Silver Creek
The Silver Creek volcanic field covers about 1600 km2 ESE of Newberry volcano and Diamond Craters. Four K-Ar dates in the eastern part of the field range from 3 to 2 million years, but the youngest rocks could be Pleistocene in age (Wood and Kienle, 1990).

Saddle Butte
The Saddle Butte volcanic field in SE Oregon consists of a 1100 km2 area of Pleistocene basalts with a superposed 240 km2 area of younger basalts. The younger flows were considered to be of possible Holocene age (Wood and Kienle, 1990), however Sherrod et al. (1989) mapped the volcanic field as Pleistocene, and a K-Ar date of 0.43 +/-0.09 million years was obtained. Oregon state Highway 78 cuts across the western side of the isolated lava field. The volcanic field is separated from the adjacent Jordan Craters field to the east by the Owyhee River and resembles the lava fields of the Snake River Plain in Idaho. Vents on the flanks of the Sheepshead Mountains at the far western end of the lava field produced lava-tube-fed flows across gently sloping terrain to the east. The most recent flow of the Saddle Butte volcanic field is known for its abundant lava tubes, including the so-called 40-Mile Cave, which is actually part of a tube system that is 13.5 km long.

Lava Butte
The Lava Butte shield volcano, also known as Rocky Butte, lies south of Jordan Craters, and is 0.03-0.09 million years old (Hart and Mertzman, 1983). The slightly older Clarks Butte shield lies to the north and has been dated at 0.25 million years. Another unnamed shield volcano lies to the east of Lava Butte.

Jackies Butte
Jackies Butte, sometimes referred to as Bowden Crater, is a small, relatively unstudied basaltic volcanic field located near the SE corner of Oregon with two small shield volcanoes and two cinder cones. Lava flows cover an area of about 325 km2 E of the Bowden Hills, SE of Burns Junction on Highway 95, and SW of Owyhee Canyon. Smith et al. (1978) estimated a probable age of less than 10,000 years, but no precise age dates have been obtained. Sarna-Wojciki et al. (1983) did not include Jackies Butte in a list of Holocene volcanic fields.

Brushy Butte
USA (California)
Brushy Butte forms a small shield complex immediately east of Timbered Crater, SSE of the Medicine Lake Highlands. The Brushy Butte complex has produced a broad apron of basaltic lava flows with fresh-looking flow features that extends preferentially down the regional gradient to the south as far as the Falls River valley. Soil development and degree of revegetation suggested a Holocene age similar to that of Hat Creek flow to the south (Peterson and Martin, 1980), and Miller (1989) also mapped Brushy Butte as Holocene. The Hat Creek flow, however, has been dated at 24,000 +/- 6000 years (Clynne and Muffler, 2010). Brushy Butte flows are overlain by the Giant Crater lava flow from Medicine Lake caldera, which has a calibrated age of 12,430 yrs BP (Donnelly-Nolan, 2010), and Brushy Butte is considered to have formed between about 12,000 and 25,000 years ago (Smith, 2014 pers. comm.).

Twin Buttes
USA (California)
A group of cinder cones near Pleistocene Burney Mountain volcano, including Twin Buttes to the SE is part of an area of extensive Quaternary volcanism north of the Lassen volcanic center. Twin Buttes at one time was considered to be of Holocene (Miller, 1989) or latest Pleistocene or early Holocene age, but Clynne et al. (2012) assigned an age of 10,000-15,000 years to Twin Buttes. Blocky, partially unvegetated lava flows extend to the north from North and South Twin Buttes, which are located at the SE foot of the Burney Mountain lava dome complex.

Silver Lake
USA (California)
Lava flows from two isolated cinder cones NW of Lassen Peak blocked drainages, forming three small lakes. The cones lie SW of Burney Mountain and WNW of MaGee Peak. Lava flows from the Silver Lake cinder cone formed Silver Lake NE of the cone and crescent-shaped Author Lake to the east and traveled 3.5 km to the SW. The crater of Silver Lake cone is open to the SW. The flat-topped Buckhorn Lake cinder cone to the SE of Silver Lake dammed up Buckhorn Lake, NE of the cone, and produced a lava flow that traveled 3.5 km to the SW. The precise age of these basaltic cones is not known with certainty. Although they lie outside the area of glaciation at Lassen, they are considered to be of comparable age to other Lassen area cinder cones of 10,000-15,000 age (Clynne, 2015, pers. comm.).

Tumble Buttes
A line of cinder cones along a NNW-SSE-trending fissure has produced a series of youthful-looking lava flows. The most prominent of these is Devils Rock Garden, a thick, blocky andesitic lava flow complex that extends to the south from Tumble Buttes. Bear Wallow Butte, the source of unvegetated lava flows on its eastern and western flanks, lies at the southern end of the chain. At the northern end is Eiler Butte, constructed on a topographic high, which has also produced blocky lava flows. The Devils Rock Garden lava flow erupted from Tumble Butte south is the youngest of the Tumble Buttes flows and was considered by Miller (1989) to be of Holocene age. The Devils Rock Garden lava flow blocks glacial outwash channels and overlies glacial gravels and thus is younger than about 15,000 years, but was mapped as latest Pleistocene by Clynne and Muffler (2010) and was estimated to have been erupted between 10,000-15,000 years ago.

Eagle Lake Field
The Eagle Lake volcanic field occupies the junction of the Cascades, Sierra Nevada, and Basin and Range geologic provinces, and consists of 15 cinder cones and basaltic lava flow vents within a larger Quaternary basaltic field. The vents are aligned along faults defining the Eagle Lake volcano-tectonic depression, and are the southernmost example of late Quaternary back-arc spreading in the NW Great Basin. The Brockman Flat lava flow, the largest of the younger flows, was erupted from a N-S oriented 3-km-long fissure vent along a fault that forms the west boundary of the Eagle Lake basin and created an approximately 63 km2 tube-fed flow field that extended across the Eagle Lake basin to the east side of Eagle Lake. Miller (1989) mapped four Holocene centers west of Eagle Lake; however, recent 40Ar/39Ar dating indicates that the youngest lava flows were erupted during a relatively short interval between about 130 and 125 ka that was unlikely to span more than a few thousand years (Clynne et al., 2017).

Coso Volcanic Field
The Coso volcanic field, located east of the Sierra Nevada Range at the western edge of the Basin and Range province consists of Pliocene to Quaternary rhyolitic lava domes and basaltic cinder cones covering a 400 km2 area. Much of the field lies within the China Lake Naval Weapons Center. Active fumaroles and thermal springs are present in an area that is a producing geothermal field. The youngest eruptions were chemically bimodal, forming basaltic lava flows along with 38 rhyolitic lava flows and domes, most with youthful, constructional forms. The latest dated eruption formed the Volcano Peak basaltic cinder cone and lava flow and was Potassium-Argon dated at 39,000 +/- 33,000 years ago. Although most activity ended during the late Pleistocene, the youngest lava dome may be of Holocene age based on geomorphological evidence (Monastero 1998, pers. comm.).

Copco Lake
Lava flows from two cinder cones near Copco Lake were dated from morphological evidence as being less than one or two thousand years old (Williams 1949), however Miller (1989) indicated that the Copco Lake volcanics are of late-Pleistocene age.

Goosenest
The Goosenest shield volcano and summit pyroclastic cone were considered by Williams (1949) to be Holocene in age, but Miller (1989) mapped it as late Pleistocene.

Whaleback
Williams (1949) mapped the Whaleback shield volcano and nearby fissure vents as Holocene in age, but Luedke and Smith (1981) mapped the area as Pleistocene and Miller (1989) did not include Whaleback in a summary of Holocene volcanism in California.

Rainbow Mountain
Rainbow Mountain, located between Mt. Shasta and Medicince Lake volcanoes, is a massive andesitic-dacitic stratovolcano of early Pleistocene age.

Hackamore
Hackamore is a large volcanic field east of Medicine Lake volcano. This Quaternary field covers an area of at least 850 km2 with at least a dozen vents, the youngest of which is about 600,000 years old (Hildreth, 2007).

Big Cave
The Big Cave shield volcano, at the northern end of an area of late-Quaternary volcanism extending north from Lassen Peak, is a small basaltic shield with young pyroclastic cones at the summit and north flank. Big Cave volcano was considered to be of either Holocene (Luedke and Smith, 1981; Miller, 1989) or latest Pleistocene or Holocene age (Sarna-Wojcicki et al., 1983). The inconspicuous low shield volcano, located between Big Lake on the north and Bald Mountain on the south, is surrounded by an extensive now forested lava field. Big Cave was considered by Clynne, 2007 pers. comm.) to probably be of similar age as nearby Cinder Butte volcano, which was dated at 38,000 +/- 7000 years.

Cinder Butte
The Cinder Butte shield volcano and flank pyroclastic cones was listed as latest Pleistocene or Holocene (Sarna-Wojcicki et al. 1983), and as Holocene by Luedke and Smith (1981) and Miller (1989). However, Clynne (in Wood and Kienle 1990) indicated Cinder Butte is slightly older than the Hat Creek lava flow, assigned an age of between 15,000 and 40,000 years (Clynne and Muffler, 2010), and Clynne et al. (2012) assigned an age of 30,000 to 50,000 years to the Cinder Butte cone cluster.

Burney Mountain
Burney Mountain, a large dacitic lava-dome complex, was active about 0.23 million years ago (Clynne, in Wood and Kienle, 1990).

Snow Mountain
The Snow Mountain volcanic center is a large eroded andesitic-to-rhyolitic stratovolcano that was active from about 2 million to 1 million years ago (Clynne, in Wood and Kienle, 1990).

Magee Peak
Magee Peak, an eroded andesitic stratovolcano, was active about 1-2 million years ago (Clynne, in Wood and Kienle, 1990). The andesitic Freaner Peak shield volcano lies across a saddle to the NE.

Blacks Mountain
Blacks Mountain, 25 km east of Hat Creek, is the most prominent of a group of andesitic shield volcanoes and is 1-2 million years old (Clynne, in Wood and Kienle, 1990).

Potato Butte
The Potato Butte cinder cone and lava field, which includes the prominent Hat Creek lava flow that traveled nearly 30 km from a fissure vent near the town of Old Station, lies immediately north of the Lassen volcanic center. Some flows are younger than the Hat Creek flow, which was initially considered to be Holocene, perhaps as young as a few thousand years (Anderson 1940), although later dating showed the the flow to be about 30,000 years old. The younger Potato Butte lavas, once considered to be of latest Pleistocene or early Holocene age, have been K-Ar dated at 65,000-75,000 years old (Clynne et al. 2000). Directly west of Potato Butte is the 61,000-year-old symmetrical lava cone of Sugarloaf Peak.

Latour Butte
Lava cone
Latour Butte, an andesitic lava cone NW of Lassen National Park, was probably active 1-2 million years ago (Clynne, in Wood and Kienle, 1990).

Caribou
The Caribou volcanic field east of Lassen National Park contains about 140 mid-Pleistocene to late-Pleistocene cones and shields that are controlled by Basin and Range extensional faulting. The Caribou volcanic field was active from about 450,000 to 20,000 years ago (Hildreth, 2007). The field includes a long, NW-SE-trending chain of Pleistocene cinder cones immediately west of Bogard Buttes.

Red Lake Mountain
A massive lava Pleistocene lava flow from Red Lake Mountain cinder cone traveled nearly 30 miles (~45 km) to the west. The basaltic flow covers nearly 50 sq miles and has an estimated volume of 1-2 cu miles (Macdonald, 1963). Highway 44 traverses the flow.

Table Mountain
Table Mountain, an andesitic stratovolcano at the NW corner of Lassen National Park, is an andesitic stratovolcano active about 1-2 million years ago. Red Lake Mountain, immediately to the NW of Table Mountain, is the source of youthful-looking basaltic and andesitic lava flows of late-Pleistocene age (Clynne, in Wood and Kienle 1990; Miller 1989).

Black Butte
Longitude: 122°W
Black Butte, a pyroclastic cone west of Lassen National Park, was thought to be of Holocene age, but later mapping indicates a late Pleistocene age (Miller 1989).

Dittmar
The Dittmar volcanic center is a massive eroded andesitic stratovolcano at the SE part of Lassen National Park that was active about 2.-5-1 million years ago (Clynne, 1990). Dacitic lava domes are located in the Hot Springs and Kings Creek canyons. The younger Mount Harkness stratovolcano lies immediately to the SE of the Dittmar volcanic center.

Sifford Mountain
Sifford Mountain, a basaltic-to-andesitic shield volcano, rises in south-central Lassen National Park. It was probably active during the past 100,000 years (Clynne, in Wood and Kienle, 1990).

Maidu
The massive, highly eroded Maidu volcano center SW of Lassen National Park was active about 2-0.8 million years ago (Clynne, 1990). The hydrothermally altered andesitic stratovolcano also has erupted rhyolitic rocks, and a dacitic lava-dome field lies on the north flank of the volcanic center.

Inskip Hill
Inskip Hill and nearby pyroclastic cones were thought to be of Holocene age, but later mapping indicates a late Pleistocene age (Miller, 1989).

Sutter Buttes
The isolated Sutter Buttes rise dramatically above the flat floor of the Sacramento Valley. This andesitic-to-rhyolitic lava-dome complex was active during the Pleistocene. An andesitic central core is surrounded by a ring of dacitic-to-rhyolitic domes.

Long Valley
The large 17 x 32 km Long Valley caldera east of the central Sierra Nevada Range formed as a result of the voluminous Bishop Tuff eruption about 760,000 years ago. Resurgent doming in the central part of the caldera occurred shortly afterwards, followed by rhyolitic eruptions from the caldera moat and the eruption of rhyodacite from outer ring fracture vents, ending about 50,000 years ago. During early resurgent doming the caldera was filled with a large lake that left strandlines on the caldera walls and the resurgent dome island; the lake eventually drained through the Owens River Gorge. The caldera remains thermally active, with many hot springs and fumaroles, and has had significant deformation, seismicity, and other unrest in recent years. The late-Pleistocene to Holocene Inyo Craters cut the NW topographic rim of the caldera, and along with Mammoth Mountain on the SW topographic rim, are west of the structural caldera and are chemically and tectonically distinct from the Long Valley magmatic system.

Big Pine Volcanic Field
The Big Pine (Aberdeen) volcanic field in the Owens Valley contains more than 40 vents over a 1000 km2 region of the Owens Valley. The basaltic field consists of cinder cones that produced lava flows up to 9 km long and a single rhyolitic lava dome. Activity was episodic throughout the Quaternary. Chesterman (1982) considers the latest activity to be of Holocene or late Pleistocene age; other sources attribute the last eruptions to the Pleistocene.

Lava Mountains Volcanic Field
Pliocene-Pleistocene (IAVCEI).

Cima Lava Field
The Cima volcanic field covers an area of about 150 km2 and contains 52 vents of Miocene-to-Pleistocene age. The youngest flows have been mapped as Holocene (Calif Div of Mines & Geol), and a radiocarbon date of 330-480 BP was obtained on the Black Tank cone. Later work suggests that the most recent activity was no younger than about 15,000 BP (Dohrenwend, in Wood and Kienle 1990; Wells et al. 1990). The youngest surface exposure ages obtained by Philipps (2003) were 11,500 and 11,600 years BP.

Amboy
The 70-sq-km Amboy basaltic lava field was erupted onto a flat-lying alluvial valley from Amboy Crater, a prominent cinder cone with four nested craters that rises 75 m above adjacent lava flows at the NE end of the lava field. The dominantly pahoehoe lava field divided the Bristol Dry Lake, occupying a depression between the Bristol and Bullion Mountains, into two playas. The cone and flow were originally considered to be early Holocene in age, but more recent surface exposure dating (Phillips, 2003) has given a 79,000 +/- 5000 yr BP age.

Pinto Basin-Salton Creek
Remnants of Pleistocene or Holocene basaltic flows and pyroclastic deposits lie on alluvium (Chesterman 1982). These volcanics are mapped as Pleistocene (Calif Div Mines & Geol, Luedke and Smith 1981).

Sinker Butte
USA (Idaho)
A Pleistocene shield volcano and tuff cone in the western Snake River Plain, Sinker Butte, is partially dissected by the Snake River Canyon. Lava flows from the tuff cone flowed up to 10 km to the south. A broad lava shield is overlain by a large tuff cone that is capped with lava flows and welded spatter. Ar-Ar dates of 1.25 and 1.17 Ma were obtained from basalts directly below phreatomagmatic tephra and capping basalts, respectively.

Mountain Home-Kuna Lava Field
USA (Idaho)
This extensive field of Quaternary basalt extends about 95 km between Mountain Home and the Kuna-Melba area southeast of the Boise River Valley (Wood, 1997). Basaltic outcrops have been dated around 2 Ma at Wild Horse Butte and Jackass Butte.

Cerro Grande
USA (Idaho)
Several late-Pleistocene lava flows were erupted near Big Southern Butte. The North Robbers flow was radiocarbon dated 11,940 +/- 300 before present (BP); the Cerro Grande flow was dated at 10,780 +/- 300 BP.

Blackfoot Lava Field
The Blackfoot Lava Field (BLF) is located in southeastern Idaho, at the margin of the Eastern Snake River Plain (ESRP). It is located within a graben of the Northern Basin and Range Province. Though it is not actually part of the ESRP, it is similar in its mineralogy, geochemistry, and bimodal volcanism (McCurry et al., 2011). However, shield volcanoes are less common than in the ESRP and more explosive volcanism appears to have been prevalent. Ages of BVF lavas are scarce, but they are believed to be similar in age to Gem Valley lavas (27.5 +/- 10 ka) (McCurry et al., 2011). In addition to the lava flows, there are three rhyolite domes, ranging in age from 58 +/- 7 ka (Heumann, 2004) to about 1.5 Ma (Luedke and Smith, 1983). Blackfoot Lava Field may be a potential geothermal resource (McCurry et al., 2011).

Menan Buttes
Tuff cone(s)
North and South Menan Buttes are the two largest of a N-S line of basaltic tuff cones formed by phreatomagmatic eruptions along the Snake River in eastern Idaho. They were considered to be very late Pleistocene, or more probably, early Recent (Holocene) by Hamilton and Myers (1963). Creighton (1987) cites mapping by LaPoint that indicates a middle to late Pleistocene age, as does King (in Wood and Kienle, 1990).

Leucite Hills
USA (Wyoming)
The Leucite Hills consist of a 2000 km2 area with less than two dozen isolated lava flows, dikes, necks and cinder cones of unusual potassium-rich composition. Their age is about 1.1 Ma.

Sheldon-Antelope
USA (Nevada)
Several Quaternary lava flows along the Nevada-Oregon border issued from small shield volcanoes. The only available Potassium-Argon age is 1.2 million years ago.

Buffalo Valley
USA (Nevada)
A group of cinder cones and lava flows in the Buffalo Valley north of the Oligocene Fish Creek Mountains caldera range in age from 3.05 to 0.92 million years ago (Dohrenwend, in Wood and Kienle 1990).

Steamboat Springs
USA (Nevada)
A small volcanic field of rhyolitic lava domes and flows about 20 km south of Reno, Nevada, ranges in age from 2.53 to 1.14 million years. No eruptive activity has occurred at Steamboat Springs during the Holocene, although it was included in the Catalog of Active Volcanoes of the World (Coombs and Howard 1960) based on its geothermal activity. The Steamboat Springs area is dotted with about 50 active hot springs, numerous steam vents, and fumaroles, and is an actively producing geothermal field.

Aurora-Bodie
Aurora-Bodie volcanic field in west-central Nevada near the California border NNE of Mono Lake contains well-preserved cinder cones and lava flows of late Pleistocene age. The most prominent feature, Aurora Crater, is a 25,000 years before present cinder cone surrounded by lava flows. Mud Spring volcano is another late Pleistocene vent with a well-preserved lava flow. Older volcanics of the field include Pliocene andesitic lava domes and Pliocene cones such as Beauty Peak and Mount Hicks.

Lunar Crater
The Lunar Crater volcanic field in central Nevada contains almost 100 Pliocene-to-Pleistocene volcanic vents cutting across the Oligocene Lunar Lake caldera. The most distinctive feature of the field is Lunar Crater, a 1-km-wide, 130-m-deep maar. Several NE-trending chains of cinder cones occur within the field, which contains lava flows up to 6 km long. The ages of the youngest lava flow, the Black Rock flow, was considered to be early Holocene (Luedke and Smith, 1981), but a cosmogenic exposure age of 38,000 +/- 10,000 years was obtained from the Black Rock flow (Shepard et al., 1995).

Clayton Valley
A solitary cinder cone in Clayton Valley NE of Silver Peak is Potassium-Argon dated about 0.39 million years ago. The breached cone has produced a 2-km-long lava flow partly buried by Quaternary alluvium (Dohrenwend, in Wood and Kienle 1990).

Crater Flat
The Crater Flat volcanic field south of the Miocene Timber Mountain caldera contains five Quaternary cinder cones and lava flows. The youngest cone, the Lathrop Wells scoria cone, was formed about 80,000 years ago (Valentine et al., 2007) and produced lava flows from vents at the southern and NE flanks of the scoria cone.

Santa Clara
USA (Utah)
A Pliocene-to-Quaternary volcanic field north of St. George in SW Utah contains numerous cinder cones and lava flows. The Santa Clara lava flow, originating from two youthful-looking cinder cones above Snow Canyon, is one of many young late-Quaternary lava flows in the Colorado Plateau/Basin and Range region. The sparsely vegetated flow traveled 16 km S down Snow Canyon, excavated through rocks of the colorful Navajo Sandstone. Estimates of the age of the Santa Clara flow have ranged widely from as young as about 1000 years. Sands beneath the flow, however, were dated by optically stimulated luminescence at about 40,000 years, and charcoal just underneath the flow at the same location was radiocarbon dated at about 27,270 +/- 250 yrs BP (Biek et al., 2010). Older Snow Canyon flows of two generations now cap mesa tops as a result of topographic inversion.

Bald Knoll
USA (Utah)
Bald Knoll is the youngest of a group of basaltic cinder cones on the SW part of the Paunsaugunt Plateau in southern Utah, between the southern end of Bryce Canyon National Park and the western margin of Grand Staircase-Escalante National Monument. The 2135-m-high Bald Knoll has a well-preserved crater and produced a massive youthful-looking lava flow that traveled about 12 km to the SSE. The olivine-basaltic flow fills the floor of Johnson Valley south of Bald Knoll and reaches beyond Ford Pasture into Johnson Canyon. No precise age for the flow is available, but although it was at one point estimated to be several hundred to several thousand years old (Gregory, 1951), Doehling (2008) noted radiometric dates of 0.34 Ma and older on adjacent lava flows and mapped all flows in this area as no younger than late Pleistocene. Buck Knoll and Black Knoll (also known as Corral Knoll) are cinder cones to the west that lie on the western side of Kanab Creek and produced lava flows that traveled as far as 22 km down the Kanab valley.

Kolob
USA (Utah)
The basaltic Kolob volcanic field on the west margin of Zion National Park contains the youthful-looking Crater Hill cinder cone and associated lava flows at the SW corner of the park and older cones to the north on the upper Kolob Plateau. The latter cones are Pleistocene in age and were erupted through the colorful rocks of the Navajo Sandstone formation, producing lava flows that extended 10-15 km down valleys to the south. Lava flows from Crater Hill blocked drainages, forming the ephemeral Coalpits and Grafton lakes. The latter extended up the Virgin River past the current town of Springdale at the southern entrance into Zion National Park. Crater Hill was at one point considered to be of probable Holocene age, but later work taking into consideration stream downcutting rates suggest an age of about 100,000 years (Biek et al., 2003). An optically stimulated luminescence date of 122.3 +/- 15.73 ka was obtained from sediments in Grafton Lake, formed by the lava flow from Crater Hill.

Mineral Mountains-Cove Fort
The Pleistocene Mineral Mountains-Cove Fort volcanic field contains silicic lava domes in the Mineral Mountains and basaltic and basaltic andesite cinder cones and lava flows of the Cove Fort and adjacent areas. The youngest flows of the Cove Fort field were considered to be of possible early Holocene age (Condie and Barsky 1972), but Potassium-Argon dates of 0.3 million years ago were obtained from the youngest flows (Nash, in Wood and Kienle 1990).

Smelter Knolls
Smelter Knolls in west-central Utah are a Pliocene rhyolitic lava dome complex. Nearby basaltic volcanism is dated at 0.31 million years ago (Nash, in Wood and Kienle 1990).

Fumarole Butte
The Quaternary basaltic-andesite shield volcano Fumarole Butte in west-central Utah is dated 0.9 million years ago. Hot springs are found on the eastern flanks (Nash, in Wood and Kienle 1990).

Willow Peak
USA (Colorado)
The Willow Peak cinder cone is located in the White River National Forest, and can be reached from Coffee Pot Road. Although geomorphically young, this cone is regarded as somewhat older than the Dotsero lava flow (about 4,000 years before present). A lava flow that traveled 5.5 km to the east.

McCoy
USA (Colorado)
A 6.5-km-long basaltic lava flow from two scoria cones is Potassium-Argon dated 0.64 +/- 0.2 million years ago (Larson et al. 1975).

Sentinel Plain
USA (Arizona)
The Sentinel Plain volcanic field covers about 600 km2 along the Gila River with basaltic lava flows. The field was active from 3.3 to possibly 1.3 million years ago (Lynch, in Wood and Kienle 1990).

Springerville Volcanic Field
USA (Arizona)
The Springerville Volcanic Field contains more than 380 vents and lava flows of Pliocene to Pleistocene age. This alkali basalt field contains cinder cones, maars and lava domes, with the youngest dated cones being 0.3 million years ago.

San Carlos
USA (Arizona)
The small San Carlos volcanic field covers about 50 km2 with basaltic cinder cone and lava flow remnants. The field, active from possibly 4.2 to 1.0 million years ago, is located within the San Carlos Apache Indian reservation (Lynch, in Wood and Kienle 1990).

Geronimo
The Geronimo (San Bernardino) volcanic field contains over 140 eruptive centers, mostly pyroclastic cones, in an area of 850 km2. The basaltic field in the SE corner of Arizona was active between 3.2 and 0.3 million years ago (Lynch, in Wood and Kienle 1990).

Potrillo Volcanic Field
USA (New Mexico)
The Potrillo volcanic field in southern New Mexico along the western margin of the Rio Grande Rift contains more than 150 cinder cones and five maars, including the Kilbourne Hole, and a small shield volcano. The southernmost maar, Potrillo maar, straddles the US-Mexico border. The Potrillo field was active from 2.65 to 0.8 million years ago (Hoffer, in Wood and Kienle 1990).

Jornada del Muerto
USA (New Mexico)
The Jornada del Muerto volcanic field in south-central New Mexico consists of a low shield that was the source of large radial lava flows. The age of the lavas is 0.76 million years ago (Crumpler and Aubele; in Wood and Kienle, 1990).

Lucero
USA (New Mexico)
The Miocene to Pleistocene Lucero volcanic field contains basaltic cinder cones, small shield volcanoes and tuff rings scattered over a 2000 km2 area. The latest eruptions took place only a few tens of thousand years ago (Baldridge, in Wood and Kienle, 1990).

Taylor Volcanic Field
Mapped as Pleistocene or Pliocene flows. Probably early Pleistocene (Lipman and Moench, 1972).

Cat Hills
The Cat Hills volcanic field west of Albuquerque contains about two dozen small cinder cones erupted along a N-S fissure, a small shield volcano and a Pliocene maar. The Cat Hills field was formed about 0.14 million years ago (Ma); the Los Lunas volcano to the SE formed between 1.3-1.1 Ma (Kudo, in Wood and Kienle 1990).

Albuquerque
The Albuquerque volcanic field was erupted along N-S fissures from about 0.17 to 0.7 million years ago, spatter cones and lava flows (Kudo, in Wood and Kienle 1990). Vulcan (or J) cone contains a lava dome split into two by an explosion crater.

Valles Caldera
The 22-km-wide Valles Caldera was formed as a result of two large-volume eruptions that created the widespread Bandelier Tuff ignimbrite plateaus on all sides of the caldera. The lower member of the Bandelier Tuff, the Otawi, was emplaced about 1.7 million years ago (Ma) and resulted in the formation of most of the present-day caldera, including the Toledo embayment at the NE side. The upper member, the Tshirege, is dated about 1.2 Ma, and also deposited voluminous welded pyroclastic flows over about the same area as the Otawi. Post-caldera volcanism has included the emplacement of multiple ring-fracture lava domes and uplift of the caldera floor, forming the Redondo Peak resurgent dome. The El Cajete Pumice, Battleship Rock Ignimbrite, Banco Bonito Rhyolite, and the VC-1 Rhyolite were emplaced during the latest eruption, about 50,000-60,000 years ago. Seismic investigations show that a low-velocity zone lies beneath the caldera, and an active geothermal system with hot springs and fumaroles exists today.

Taos Plateau
The massive Taos Plateau volcanic field covers an area of 7000 km2 along the Rio Grande Rift in north-central New Mexico and was active from about 10 million to 1.8 million years ago. The Red Hill lava flow is of probable Pleistocene age (Dungan et al., 1989).

Ocate
The Ocate (Mora) volcanic field is part of the Jemez Lineament and located east of the Rio Grande Rift in northern New Mexico. It contains numerous basaltic to dacitic flows and cinder cones over a 90 km2 area. The field was active from 8.3-0.8 million years ago, although most activity ended by the Pleistocene (Baldridge, in Wood and Kienle 1990).

Raton-Clayton
The Raton-Clayton volcanic field is a large Miocene-Quaternary field stretching from near Trinidad, Colorado to Clayton, New Mexico. The main pulse of volcanism took place between 4 and 1.8 million years ago. The relatively youthful-looking Capulin Mountain cinder cone was considered to have been active during the Holocene, based on stratigraphic correlations of its lava flow with distant alluvial sequences. However, later work indicated the lava flow was more than 22,000 years old. More-recent cosmogenic helium dating gave an age of 59,100 years for the lava flow (Sayre et al., 1995), who site additional geomorphological evidence for a Pleistocene age for Capulin Mountain. Several other cones and vents nearby, such as Baby Capulin, Twin Mountain, and the Purvine Mesa vents, are younger than Capulin Mountain (Dungan et al. 1989). Although they were erupted during the same geomorphologic period as Capulin Mountain, their precise age is not known.

Vance Segment
Pacific Ocean (northern)
The entire Juan de Fuca Ridge is an active spreading center, though there have been no eruptions observed or dates along the Vance Segment. This segment lies between Cleft Segment (the southern-most of the JdfR) to the south, and Axial Seamount to the north.

Central Segment
Pacific Ocean (northern)

Phoenix Segment
Pacific Ocean (northern)

Kaena
Hawaiian Islands
Water discoloration, sulfur odor, possible boiling water, and possible minor floating pumice were observed 60 km NW of the tip of Oahu on 22 May 1956. The seamount at that location has a depth of about 1200 m at the end of the Kaena Ridge. Macdonald (1959) suggested that a submarine eruption may have occurred, but noted that evidence is less certain than that for the 1955 report of a submarine eruption near Necker Island.

Kohala
Hawaiian Islands
The oldest of the volcanoes comprising the island of Hawaii, Kohala forms an oval shield constructed along two NW-SE trending rift zones at the NW tip of the island. Large valleys cut into the NE flanks, including the dramatic Waipio Valley, correspond to the headwall region of the massive Pololu debris avalanche that extended 130 km NE. A caldera that apparently formed during the shield stage was buried by post shield lavas. The youngest volcanic series (the Hawk volcanics) are Potassium-Argon age dated between 0.26-0.06 million years ago.

Kahoolawe
Hawaiian Islands
The uninhabited island of Kahoolawe, SW of the island of Maui, consists of a broad, low basaltic shield volcano formed by Pleistocene eruptions along a rift zone that extends SW from a buried, 5-km-wide caldera at the eastern side of the island. The eastern rim of the caldera lies beneath the waters of Kanapou Bay. Two less prominent rift zones trend to the east and north. Much of the island is truncated by steep sea cliffs that expose the thin lava flows making up the volcano. Stearns (1946) and Macdonald and Abbott (1970) considered cinder cones within the caldera on the west side of Kanapou Bay to be of Holocene age, but this age was considered probably too young by Langenheim and Clague (1987), who mapped the cones as Pleistocene or Holocene. Sano et al. (2006) obtained K-Ar dates on the youngest flows of 900,000 to 980,000 years Before Present.

Mahukona
The Pleistocene Mahukona seamount lies between the islands of Hawaii and Kahoolawe, NW of Hualalai volcano. The distinct cone is about 4 km in diameter.

West Maui
The Pleistocene West Maui shield volcano is deeply dissected by spectacular steep-sided valleys that extend from the north and east into the summit caldera. Late-stage cinder cones and lava flows on the W flank were mapped as Recent by Stearns (1946). Mullineaux et al. (1987) indicated that the youngest lava flows are more than 25,000 years old, and the youngest K-Ar dates obtained are older than one million years (Sherrod et al., 2007).

Lanai
The Pleistocene Lanai shield volcano was constructed along three rift zones, the most prominent of which is the NW rift zone. The large submarine Clark debris avalanche extended 150 km S (Moore et al. 1989). A caldera is located at the southern end of the island. Lava and spatter cones were formed along the rift zones. A single Potassium-Argon date of 1.28 +/- 0.4 million years ago has been obtained on Lanai basalts.

East Molokai
East Molokai volcano was constructed along an E-W trending rift zone. The northern half of the volcano is truncated by a cliff more than 1 km high resulting from the massive Wailau debris avalanche that extended more than 100 km N (Moore et al. 1989). The youngest eruptive products formed the small Kalaupapa shield volcano that created a peninsula off the north coast between about 0.57 and 0.35 million years ago (Langenheim and Plague 1987).

West Molokai
The flat West Molokai shield volcano was formed by eruptions along two rift zones at the west end of Molokai Island during the Pliocene and early Pleistocene. The youngest Potassium-Argon date is 1.52 +/- 0.6 million years ago (Langenheim and Clague, 1987).

Koolau
The extensively eroded, elongated Koolau basaltic shield volcano of Pliocene-to-Pleistocene age forms much of the eastern half of Oahu Island. A lengthy NW rift zone is defined by a dike complex that runs the length of the windward coast. The largest documented submarine landslide of the Hawaiian islands produced the Nuuanu debris avalanche, which traveled 230 km NE from its source at the Nuuanu Pali on the NE side of the volcano. After a period of long quiescence activity resumed, forming the Honolulu volcanic series at the SE end of Oahu. The youngest members of the Honolulu Series, which consists of a group of tuff cones, maars, cinder cones, and spatter cones, many with associated lava flows, were considered by Stearns (1946) to be about 5000 years old. The youngest radiometric dates, however, ranged from 31,000 to 43,000 years old (Mullineaux et al., 1987), and more recent work (Ozawa et al., 2005) dated material to about 40,000 years. Sherrod (pers. comm., 2006) noted that earlier estimates of Holocene ages have been shown to be incorrect, and that the Sugarloaf lava flow, thought to be younger than 10,000 years, was dated at 110,000 years.

Waianae
The elongated Waianae shield volcano forms much of western Oahu Island. The Waianae Slump, a landslide formed during multiple events, extends 90 km SW (Moore et al. 1989). The heavily eroded volcano was largely formed during the Pliocene, but late-stage Kolekole volcanics at the SE end of the range are considered to be of Pleistocene age (Langenheim and Plague 1987).

Kauai
Kauai Island is composed of a single large eroded shield volcano with a summit caldera 15-20 km in diameter and two flank calderas. Large Pliocene debris avalanches extended to the north and south. The spectacular Waimea Canyon and Napalm cliffs on the NW coast are products of extensive erosion. Most of the volcano is of Pliocene age; however, rejuvenation of activity during the Pleistocene produced lavas and cones over the eastern two-thirds of the island Potassium-Argon dated 1.40-0.6 million years ago (Macdonald and Abbott 1970).

Niihau
Niihau is the eroded remnant of a Miocene to Pliocene shield volcano. Rejuvenation during the late Pliocene and Pleistocene produced a series of small shield volcanoes, cinder cones and tuff cones.

Kaula
Ka'ula Island is a Pleistocene tuff cone that rests on a broad submerged shield volcano (Macdonald and Abbott, 1970; IAVCEI, 1973).

Hiva Oa
Pacific Ocean (central)
The Marquesas Islands show an age progression with the youngest volcanoes occurring at the SE end of the chain. Hiva Oa, a large shield volcano with a caldera truncated on the south side, is the NW-most volcano of the chain with some Pleistocene activity. Potassium-Argon dates range from 2.48-1.58 million years ago (Duncan and Mcdougall 1974). Radiometric ages for Tahuata Island, immediately south of Hiva Oa, are Pliocene.

Fatu Hiva
Pacific Ocean (central)
Fatu Hiva is the SE-most and youngest of the Marquesas Islands. Potassium-Argon dates for the island, a shield volcano with a large summit caldera truncated on the west, range from 1.39-1.30 million years ago (Duncan and Mcdougall, 1974).

Moorea
Pacific Ocean (central)
Like several other central Pacific island chains, the Society Islands are progressively younger to the SE. Moorea, the NW-most of the Society Islands with Pleistocene volcanism, is a dissected shield volcano whose caldera is open to the north and surrounded by sharp-topped peaks. Potassium-Argon dates for the island range from 1.64-1.49 million years ago (Duncan and Mcdougall 1976).

Tahiti-Nui
Tahiti-Nui is the larger of two coalescing shield volcanoes forming the island of Tahiti. Much of the original volcano is intact; the central caldera is drained to the north by the Papenoo River. Potassium-Argon dates range from 1.23-0.48 million years ago (Duncan and Mcdougall, 1976).

Tahiti-Iti
The smaller and younger of two coalescing shield volcanoes on Tahiti, Tahiti-Iti (Taiarapu) is connected to Tahiti-Nui by a narrow isthmus. Potassium-Argon ages range from 0.48-0.38 million years ago (Duncan and Mcdougall 1976).

Aitutaki
Volcanic rocks of Aitutaki Atoll in the Cook Islands are Potassium-Argon dated 0.77-0.66 million years ago (Duncan and Mcdougall 1976).

Rarotonga
Potassium-Argon dates from the Rarotonga shield volcano in the Cook Islands range from 1.8-1.2 million years ago (Duncan and Mcdougall 1976).

Rurutu
Rurutu is an eroded shield volcano in the Astral (Tubuai) Islands capped by later Pleistocene lava flows that reached the sea through gaps in the fringing coral reef. The younger volcanics are Potassium-Argon dated from 1.85-1.05 million years ago (Duncan and Mcdougall 1976).

Pitcairn
Located at the SE end of the Duke of Gloucester-Gabbier Islands chain, Pitcairn is a small island remnant of a shield volcano with a dissected caldera. Potassium-Argon dates range from 0.95-0.45 million years ago (Duncan et al. 1974).

Pacific Ocean (southern)
A basalt dredge sample Ar-Ar dated by Koppers et al. (2004) was 1.110 +/- 0.055 Ma. This seamount is about 90 km NW of Lonsdale Seamount and 400 km N of the Hollister Ridge 1991 acoustic signal location. It is near the extreme eastern end of the Louisville Seamount Chain where it intersects the Pacific?Antarctic Ridge, near where some models locate the Louisville hotspot (Vlastelic and Dosso, 2005).

Cerro Leon
Mexico
Cerro León, also known as Volcán Prieto ("Dark volcano"), is a small, roughly 280-m-high cone of early Pleistocene age (~2.5 Ma) that was constructed along the Guaymas lineament on the east coast of northern Baja California (Martin-Barajas and Weber, 2003). The eastern flank of the volcano extends into the Gulf of California. It is part of the Puertecitos Volcanic Province, within the Gulf of California Rift Basin System (Martin-Barajas and Weber, 2003; Oskin and Stock, 2003). This volcanic province is the most extensive in the region and has the longest known volcanic history. It is typically calc-alkaline and largely rhyolitic, but Cerro Leon is predominantly andesitic (Stock, 2000; Gastil et al., 1979; Martin-Barajas and Weber, 2003).

San Ignacio Volcanic Field
Mexico
The San Ignacio volcanic field lies north of the town of the same name and east of the town of Vizcaino. Miocene tholeittic basaltic-andesitic lava flows and somewhat magnesian Pliocene-to-Pleistocene andesites emitted from dozens of cinder cones overlie Tertiary sediments (Pallares et al., 2007; Calmus et al., 2003). Surface morphology implies that these Plio-Pleistocene flows were likely highly viscous, compared to their more fluid Miocene counterparts (Pallares et al., 2007). The San Ignacio field dates to about 0.65 to 5 Ma; most of the volcanic activity at this center occurred during the Miocene and early Pliocene (Calmus et al., 2003).

El Aguajito
Mexico
El Aguajito caldera (also known as Santa Ana caldera) is located along the Gulf of California immediately NE of Tres Vírgenes volcano and NW of La Reforma caldera. The rim of the approximately 10-km-wide resurgent caldera is not exposed, but an arcuate line of andesitic-to-rhyolitic lava domes covers its northern margin. Formation of the rhyolitic caldera was associated with the eruption of ignimbrites, K-Ar dated at 0.76 +/- 0.06 million years ago (Ma), most of which were deposited in the Gulf of California. Rhyolitic lava domes on the northern margin have been dated at 0.5 +/- 0.04 Ma; dacitic lava domes on the southern side of the caldera appear to be older. The regional NNE-SSW-trending Cimarron fault cuts across the center of the caldera. Hot springs are located along the southern caldera margin, and active seismicity was noted during geothermal exploration.

Punta Pulpito
Punta Púlpito is a Pleistocene obsidian dome dated at about 0.5 million years that forms a small peninsula along the Gulf of California, east of the southern tip of Bahía Concepción in southern Baja California. The Saquicismunde geothermal area with hydrothermal springs and steaming ground lies close to the dome, and the larger Los Volcanes geothermal area, lying along the coast about 5 km S, contains 18 fumaroles along a NW-SE alignment.

Cerro Mencenares
The Cerro Mencenares volcanic complex along the Gulf of California is situated at the northern extent of the Loreto Basin, SE of Bahia Concepcion (Dorsey and Umhoefer, 2000). It's eruptive history, which involves three eruptive events, likely played a role in the development of the Loreto Basin. Cerro Mencenares itself is a large stratovolcano; the complex consists of this composite cone and several peripheral centers that cover an area of about 150 km2 (Bigioggero et al., 1995). The volcanic products generally consist of Pliocene to lower Pleistocene andesitic to rhyolitic domes, flows, and pyroclastics (San Juanico Unit), along with dacitic and andesitic-basaltic lava flows (Mencenares Unit) (Dorsey and Umhoefer, 2000; Bigoggero et al., 1995). Younger silicic domes and minor basaltic lava flows make up the San Basilio-San Juan Unit (Bigioggero et al., 1995). The volcanic tuffs and breccias on the flanks of the complex are often interbedded with marine mudstones and limestones (Bigioggero et al., 1995; Dorsey and Umhoefer, 2000).

La Reforma
The early Pleistocene La Reforma caldera lies along the Gulf of California immediately east of Tres Vírgenes volcano and SE of the late-Pleistocene El Aguajito caldera. The roughly 10-km-wide caldera contains basaltic, andesitic, and dacitic lava flows, and rhyolitic lava domes. A prominent arcuate caldera rim extends from La Reforma along the NW coast to near Punta Las Cuevas on the SE coast. The age of the caldera was determined by the K-Ar method to be between 1.6 and 1.4 million years old (Ma). A 1.09 +/- 0.11 Ma age was obtained on a ring-fracture lava dome. Andesitic lava flows were erupted on the flanks of the caldera both before and after caldera formation.

Moctezuma Volcanic Field
The Moctezuma volcanic field occupies a 380 km2 area along the foothills of the Sierra Madre Occidental in NW México. An early stage of tholeiitic basaltic volcanism originating from fissures along the eastern boundary of the graben produced a broad mesa within a large graben in the Moctezuma Basin. Younger alkalic basaltic volcanism produced five scoria cones concentrated along a crudely N-S trend in the center of the graben. These produced lava flows that traveled primarily SW. The youngest cone is Cerro Blanco, which produced lava flows to the SW and was Potassium-Argon dated at about 0.53 +/- 0.2 million years.

Camargo Volcanic Field
The Camargo volcanic field is located in the northern Bolsón de Mapimí graben in north-central México, about 150 km SW of Big Bend National Park in Texas. More than 300 volcanic vents, mostly cinder cones and lava cones, are located in a broad 2500 km2 lava plateau that extends 60 km E-W and 70 km N-S. It is mostly Pliocene in age, but an early Pleistocene age of 1.43 +/- 0.05 Ma was obtained on one sample. The best-studied vent of the field is 1.63 Ma Cerro el Salto (also known as La Olivina), a cinder cone whose spinel-lherzolite xenoliths were once mined for peridot.

Aldama Volcanic Field
An area of Quaternary phonolitic and basaltic pyroclastic cones and lava flows is located along the Gulf of Mexico SE of the Sierra de Tamaulipas. Trachytic and phonolitic eruptions were followed by the emission of young basaltic lava flows from cinder cones. Scattered areas of Tertiary or Quaternary volcanic rocks also lie along a NNW-SSE-trending line on the coastal plain east and NE of the Sierra de Tamaulipas and in areas farther west toward the base of the mountain range.

Los Flores
The Tertiary-to-Quaternary Los Flores volcanic field is located in the rugged limestone peaks of the Sierra Madre Oriental at the conjunction of the states of Tamaulipas, Nuevo León, and San Luis Potosí in eastern México. Basaltic lava flows of the Mexican Basin and Range Province erupted in the valleys formed by late-Mesozoic faulting and folding that formed the NNW-SSE-trending Sierra Madre Oriental. One massive youthful, but undated Quaternary pahoehoe lava flow traveled about 80 km to the SSE down a synclinal valley from Cerro Partido.

Santo Domingo Volcanic Field
The Santo Domingo volcanic field lies in the center of the state of San Luis Potosí in the southern Basin and Range province of central México. Located about 50 km NE of the Ventura volcanic field, Santo Domingo consists of a group of four maars in the NW part of the field, along with several alkalic cinder cones and associated lava flows to the SE. The largest maar, La Joya de los Contreras, is 750 x 1000 m in diameter. The Santo Domingo maars are the source of mantle-derived spinel-lherzolite xenoliths and deep-crustal granulite xenoliths.

Ventura Volcanic Field
The Ventura volcanic field consists of a group of maars and pyroclastic cones located immediately NE of the city of San Luis Potosí in the southern Basin and Range province of central México. The largest and best-known maar is La Joya Honda, a 850 x 1100 m wide, 300-m-deep maar erupted through Cretaceous limestones about 1.1 million years ago. The maars, located near the southern end of the Basin and Range province, are known for their mantle-derived spinel-lherzolite xenoliths and deep-crustal granulite xenoliths. A 10-km-long lava flow also rich in lherzolite xenoliths was erupted from the Cerro Verde cinder cone north of La Joya Honda.

San Juan
Volcán San Juan, the NW-most major volcano of the Mexican Volcanic Belt, overlooks the city of Tepic, the capital of Nayarit state. The northernmost of two twin stratovolcanoes is truncated by a 1 x 4 km wide, oval-shaped caldera formed about 15,000 years ago during an eruption that produced thick rhyodacitic pumice-fall deposits. These are up to 9 m thick beneath Tepic and extensively quarried. This major explosive eruption was followed, probably shortly thereafter, by intra-caldera eruptions of andesitic lava domes and flows. Cerro Alto stratovolcano, the 2240 m high point of the San Juan volcanic complex, is an older volcano that rises immediately to the south of San Juan. Reports of historical eruptions of San Juan in 1742 and 1859 are unconfirmed or incorrect (Luhr, 2000).

Las Navajas
Volcán Las Navajas is a low-profile shield volcano located immediately north of the more prominent Sangangüey volcano. Las Navajas is truncated by a 4-km-wide circular caldera, associated with eruption of the Las Cuevas ash. The caldera is filled by pantelleritic lava flows that overtopped the caldera rim on the north, east, and SW sides. A major plinian eruption about 200,000 years ago produced widespread airfall pumice and welded pyroclastic flows (collectively known as the La Moderna ash) that first formed a 1-km-wide central crater at the summit of a stratovolcano constructed in the center of Las Navajas caldera and then formed an elliptical caldera 2.5 x 4 km in size on the southern side of the volcano. Two cinder cones and an associated lava flow were subsequently erupted on the northern flank of Las Navajas, and Sangangüey volcano was constructed on the southern flank, largely burying the southern rim and floor of the second caldera.

Santa Maria del Oro
Maar
The scenic lake-filled Santa María del Oro maar lies between Sangangüey and Ceboruco volcanoes in the Tepic-Chapala graben. The topographically indistinct outer flanks of the maar give little hint to the dramatic 400 m drop into the Laguna Santa María crater lake. The roughly 3-km-wide maar was erupted through older Miocene rhyolitic ashflow tuffs of the Sierra Madre Occidental. Little is known of the geology or age of Santa María del Oro, but it occurs near the alignment of cinder cones extending from Sangangüey and may have a similar Pleistocene age. Pyroclastic-surge deposits from Santa María del Oro occur in valleys to the north and in some cases along the walls of the crater.

Tepetiltic
Volcán Tepetiltic is a 2020-m-high andesitic and dacitic stratovolcano, truncated by an elliptical, 5 x 2.5 km caldera that contains a lake at its NE corner. The Tepetiltic caldera has steep-sided, scalloped walls that are elongated in a NE-SW direction. The caldera originated during a major rhyodacitic eruption that produced a blanket of plinian-airfall, pyroclastic-flow, and pyroclastic-surge deposits that surrounds the volcano. Caldera collapse was closely followed by emplacement of lava domes on the eastern flank. Two andesitic domes were later emplaced on the caldera floor, and chemically unrelated flank cinder cones were erupted.

San Pedro
The elliptical 7 x 10 km wide San Pedro caldera, located immediately south of the Tepetiltic caldera, is partially filled by the three coalescing Cerro San Pedro lava domes. Construction of a large number of lava domes SE of the current location of San Pedro during the Pleistocene was followed by caldera formation associated with eruption of the Cuastecomate Pumice. The rim of the caldera, which was considered to have formed between about 450,000 and 283,000 years ago, is exposed only on the east side. The dacitic San Pedro lava domes are aligned along a WNW-trending fracture and have been potassium-argon dated at about 41,000 years. Two of the domes have collapsed, forming debris-avalanche deposits that extend as far as 10 km to the NW and SE.

Los Volcanes
A mostly Pliocene volcanic field is located near the town of Los Volcanes, at the southern end of the Atenguillo graben in the Jalisco tectonic block of western México. The 285 km2 field consists of lava cones and flat-topped flows overlying Cretaceous ignimbrites. The youngest products are earliest Pleistocene in age (Potassium-Argon date of 1.56 Ma). The extensional tectonic setting, in a graben of the Jalisco block, has resulted in the eruption of a wide variety of lava types, ranging from potassic minettes and leucitites to calc-alkaline basalts and andesites.

Northern Atenguillo
An extensive Plio-Pleistocene volcanic field is located at the northern end of the Atenguillo graben in the Jalisco tectonic block of western México. Pleistocene volcanism has occurred at two locations at the southern and northern ends of the field. Potassium-Argon ages of 0.65 and 0.67 Ma (million years) were obtained from the Las Laja shield volcano at the southern end of the volcanic field. Initial phreatomagmatic eruptions at La Laja produced pyroclastic-surge and airfall deposits associated with formation of a tuff ring or tuff cone. Subsequently the extrusion of a thick sequence of lava flows formed the symmetrical shield volcano. The flows blocked the Río Atenguillo, forming an ephemeral 20-km-long lake, and the initial flows produced pillow lavas. El Rosario, the northernmost known Pleistocene vent of the Atenguillo graben, forms an alkali-basaltic lava plateau and has a Potassium-Argon age of 0.64 Ma.

Tequila
Volcán Tequila is an eroded andesitic-dacitic volcano surrounded by a series of older flank rhyolitic lava domes and obsidian flows ranging from 0.9 to 0.23 Ma in age. A prominent summit spine, similar to that at Sangangüey, has been dated at 0.21 Ma. The spine occupies a large summit crater open to the NE, which was formed by erosion. After the cessation of activity at the central vent, andesitic lava flows were erupted from vents on the flanks, and a chain of lava domes was formed on the SE flank. At least a dozen cinder cones younger than the central volcano were erupted along a WNW-trending line SW and south of the volcano. These were roughly estimated on the basis of morphology to be older than 40,000 years.

Northern Guadalajara Mesa
A cluster of rhyolitic lava domes lies on the northern end of the Guadalajara Mesa about 20 km north of the city of Guadalajara. This area is located just beyond the SW end of the Jalpa Graben and lies along the boundary between the Pliocene-Quaternary Mexican Volcanic Belt and the mid-Tertiary Sierra Madre Occidental volcanic province. The Northern Guadalajara Mesa lava domes were erupted through Pliocene ignimbrites forming the mesa. The highest of the domes is 1820-m-high Cerro Jacal de Piedra, which lies south of Cerro el Chicharrón. A K-Ar age of 1.4 million years was obtained by Spinnler et al. (2000) from Cerro el Chicharrón. Two other domes are located along a north-south-trending line to the east.

Sierra la Primavera
The Sierra la Primavera volcanic complex is located immediately west of México's second-largest city, Guadalajara. Following the eruption of rhyolitic lava flows and domes beginning about 120,000 years before present (BP), an 11-km-wide caldera was formed as a result of the eruption of the 20 km3 Tala Tuff about 95,000 BP. La Primavera caldera subsequently filled with water, forming a lake, through which several lava domes were emplaced. The eruption of a series of domes along the margin of the caldera about 95,000 years ago was followed about 75,000 years ago by the eruption of a younger series of ring domes. Uplift and sedimentation filled the lake, and a final series of lava domes was erupted along the southern margin of the caldera beginning about 60,000 BP, with the youngest dome dated at about 30,000 BP. Steam vents and hot springs currently are active throughout the volcanic complex.

Southern Guadalajara
A chain of nine basaltic-andesite volcanic centers of Plio-Pleistocene age was constructed along a NW-SE-trending line through the southern portion of the city of Guadalajara. The centers range from small cinder cones, such as Cerro San Bartolo, to larger composite volcanoes. The westernmost cones are partially overlapped by southern Guadalajara's streets and buildings. The largest volcanoes are located at the SE end of the chain. Cerro el Papantón de Juanacatlán marks the SE end of the chain. The small stratovolcano Cerro el Molino was constructed SE of Cerro el Papantón de Juanacatlán. It is offset slightly to the south of the trend of the rest of the chain, south of a fault block of the Chapala graben.

Acatlan Volcanic Field
The Acatlán volcanic field, located SW of La Primavera caldera, is a group of andesitic cones, rhyolitic lava domes, and lava flows associated with a caldera system. The Acatlán Ignimbrite is a compositionally zoned rhyolitic-to-andesitic tuff that covers an area of about 150 km2. The ignimbrite overlies andesitic breccias dated at 0.65 million years. Following eruption of the ignimbrite, a series of rhyolitic and dacitic lava domes and andesitic cinder cones and lava flows were erupted throughout the Acatlán volcanic field.

Volcan el Cantaro
Volcán el Cántaro is the northernmost of a chain of volcanoes rising above the floor of the Colima rift zone. Cántaro, with Potassium-Argon ages ranging from 1.7 to 1.0 million years, is the oldest volcano of the Cántaro-Colima volcanic complex, which extends south through Nevado de Colima to the historically active Volcán de Colima. Cántaro is erosionally modified, but has many well-preserved andesitic-dacitic lava domes on its northern and eastern flanks. The biotite-bearing rocks of Cántaro contrast to the more mafic biotite-free rocks of Nevado de Colima and Volcán de Colima. The southward-migrating volcanism of the Cántaro-Colima chain is also reflected by a southward-younging progression at Cántaro itself.

San Sebastian Volcanic Field
The San Sebastián volcanic field, near the old silver-mining town of San Sebastián, is the northernmost of a belt of potassic volcanic fields located west of the main volcanic chain of western México. These geochemically unusual volcanoes owe their existence to their location at the conjunction of tectonic regimes involving the rifting of the Jalisco tectonic block and the subduction of the Rivera plate. The San Sebastián volcanic field consists of a group of scattered lamprophyric cinder cones erupted predominately through silicic ash-flow tuffs of the southern Sierra Madre Occidental province. The cinder cones and related lava flows, which erupted in a rugged and sparsely populated mountainous area that makes access difficult, range in age from 0.48 to 0.26 million years.

Los Azufres
The Los Azufres volcanic center is one of several silicic volcanic complexes with active geothermal systems that lie north of the axis of the Mexican Volcanic Belt. Located about 200 km NW of Mexico City, the Los Azufres center consists of a 18 x 20 km wide early Pleistocene caldera that was later partially filled by resurgent dacitic-to-rhyolitic lava domes. Two magmatic cycles lasting about 200,000 years each took place between 1.4 and 0.8 Ma (million years), consisting of silicic, followed by basaltic volcanism. The latest magmatic cycle, beginning about 0.6 Ma, involved resurgent doming of the southern part of the caldera, the eruption of chemically diverse basaltic-to-rhyolitic products, and the emplacement of dacitic-rhyolitic lava domes. The latest paroxysmal eruptions produced ignimbrites between 38,000 and 26,000 years ago. Hot springs and fumaroles are located along E-W-trending faults, and Los Azufres is an active producing geothermal field.

Apan-Tezontepec
A large volcanic field of Mesozoic to late-Pleistocene age occupies the central part of the Mexican Volcanic Belt in the NE part of the Valley of Mexico. The Apan-Tezontepec volcanic field covers portions of the states of Hildalgo, Tlaxcala, and México and contains about 300 eruptive centers. The vast majority of these are scoria cones, but shield volcanoes, lava flows, and lava domes are also present. The location of the vents is influenced by regional normal faults. Two of the largest Quaternary volcanoes of the Apan-Tezontepec volcanic field are Chiconautla and 3100-m-high Cerro Gordo, which rises immediately NE of Mexico City. The Tizayuca volcanic field lies at the NW corner of the Apan-Tezontepec volcanic field.

Tláloc
Tláloc volcano, at the far northern end of a volcanic chain stretching northward from Popocatépetl, is a 4120-m-high stratovolcano of Pliocene-Pleistocene age. Although typically considered to be the oldest volcano of the chain, recent work has documented a major plinian-subplinian eruption radiocarbon dated at about 31,500 years before present. The eruption produced a major pumice-fall deposit and associated pyroclastic flows.

Telapón
Telapón is a large stratovolcano of Pleistocene age north of Iztaccíhuatal volcano. It lies along a N-S-trending volcanic chain extending from Popocatépetl volcano that is perpendicular to the trend of the Mexican Volcanic Belt. A dacitic lava flow at the summit of the 4080-m-high volcano was K-Ar dated at about 274,000 years (Cadoux, 2007 pers. comm.).

Acoculco
The Acoculco volcanic complex lies in the NE part of the Mexican Volcanic Belt, where it intersects the Sierra Madre Oriental volcanic province. The Acoculco caldera complex is located about 80 km WNW of the better known Los Humeros caldera. Three major pyroclastic flows were erupted during the late Pliocene and Pleistocene, associated with two circular depressions 28 x 34 and 16 x 21 km in diameter, respectively. The large rhyolitic Cerros las Tetillas lava dome was emplaced during the early Pleistocene. The latest activity consisted of the extrusion of basaltic lava flows during the late Pleistocene. Thermal areas are located within the caldera complex and on its eastern flanks, and the caldera has been considered as a potential area for geothermal development.

Cerro Grande
A group of lava domes and pyroclastic cones of Pleistocene age is located on the western side of Cerro Grande, a Miocene caldera north of La Malinche volcano. Pyroclastic-flow deposits within the caldera are those of the Xáltipan ignimbrite, which originated from Los Humeros caldera to the east about 0.45 Ma (million years ago). A Potassium-Argon age of 0.49 Ma was obtained for the lava domes at Cerro Grande. Post-caldera Pleistocene activity at Cerro Grande covered a broad area on the SW-NW side of the caldera, producing andesitic and dacitic lava domes and basaltic lava cones and pyroclastic cones.

Poza Rica
Pleistocene lava flows cover a broad area between Huauchinango in the Sierra Madre Oriental and the city of Poza Rica along the Gulf of Mexico coastal plain. The basaltic and hawaiite lava flows fill valleys to depths of several hundred meters and are almost continuous from Huauchinango to Poza Rica. Possibly correlative lava flows are located in the Metlaltoyuca area to the NW of Poza Rica. K-Ar ages for these lava flows range from 1-64 to 1.31 million years (Ferrari et al., 2005).

San Martin Pajapan
San Martín Pajapan is a composite volcano at the SE end of the Sierra de Santa Martha along the Gulf of Mexico SE of Lake Catemaco. Von Wolff (1929) reported Indian traditions of "smoke" and fire from the volcano, but Nelson and Gonzalez-Caver (1993) noted that the volcano is capped by thick lateritic soils and lacks evidence for recent activity. A K-Ar date of 1.5 +/- 0.2 million years ago (Ma) was obtained from one of the youngest lava flows. K-Ar dates on the adjacent eroded volcanoes of Santa Martha and Yohualtajapan to the NW range from 3.3 to 1.0 Ma. The summits of both these volcanoes are truncated by large depressions open to the north of erosional and slope failure origin. Hundreds of partially eroded cinder cones dot the southern slopes of the Sierra de Santa Martha.

Apas-Navenchauc
The 2.9-km-wide Apas caldera was the source of block-and-ash flows, pumice flows, and ash flows that extend primarily to the SW and NW. The SW deposit forms a large fan covering about 140 km2. Deposits from the Apas collapse structure were K-Ar dated at about 0.432 million years. The 1.34-km-wide Pleistocene Navenchauc explosion crater lies immediately NE of the Apas caldera. The Navenchauc lava dome was constructed on the northern rim of the Navenchauc caldera.

Huitepec
The Huitepec lava dome lies immediately west of the city of San Cristóbal de las Casas. The hornblende-andesitic dome has a height of about 520 m and was the source of ash-flow deposits, which crop out about 5 km NW of San Cristobal. These products are generally gray in color, with a phaneritic texture and coarse grains of plagioclase, pyroxene, and amphibole (Mora et al., 2007). The base of the dome has a mean diameter of 5.18 km, covering an area of about 21.2 km2 (Mora et al., 2007). A K-Ar date of about 850,000 years was obtained from the dome. In general, Huitepec dates to about 0.85-1.95 Ma (Mora et al., 2007). Huitepec's composition, like that of other eruptive centers in the Chiapanecan Volcanic Arc, is mostly intermediate, calc-alkaline (Mora et al., 2007).

Mispia
The Mispía lava dome lies near the center of a cluster of a half-dozen Pleistocene domes SSE of the city of San Cristóbal de las Casas. The Amahuitz lava dome lies to the NE of Mispía, La Iglesia dome to NNW, La Lanza to the west, and Santontón and Venustiano Carranza domes to the south.

Siete Orejas
Guatemala
Siete Orejas is an andesitic stratovolcano with a large caldera breached to the south. The volcano overlooks Quetzaltenango, Guatemala's second largest city. The broad irregular summit profile gives the volcano its name, which means "seven ears." The latest eruption of Siete Orejas produced a widespread airfall-pumice and pyroclastic-flow deposit that is stratigraphically constrained to have been formed between 126,000 and 85,000 years ago. Volcán Chicabal, located immediately west of Siete Orejas, was constructed within a 4-km-wide breached scarp of unknown origin. This stratovolcano of unknown age has a well-preserved summit crater containing a crater lake.

Santo Tomas
Guatemala
Volcán Santo Tomás (also known as Volcán Pecul) is a large eroded stratovolcano located across a valley SE of Santa María volcano. The summit is capped by late-Quaternary andesitic tephra. A winding ridge connects it to Volcán de Zunil, 4.5 km NE, a stratovolcano that forms the topographic high point of the Santo Tomás-Zunil complex. Solfataras and thermal springs are located on the ridge's W side. Volcán de Zunil is located on the SW rim of the 4-km-wide, 600-m-deep Tzanjuyub caldera, which is breached to the S by the Río Masa. Several dacitic-rhyolitic lava domes are located on the caldera's N flank and the NW flank of Volcán de Zunil. The youngest dome, Cerro Zunil, was last active about 84,000 years ago (K-Ar dating). No Holocene eruptions at Santo Tomás are known, although the volcano was included in the Catalog of Active Volcanoes of the World (Mooser et al., 1958) based on its geothermal activity.

Cuxliquel
Guatemala
A Quaternary lava-dome complex lies in the center of a semi-arcuate depression of uncertain origin near the city of Totonicapán. A small symmetrical lava dome, Cerro de Oro, is located on the ESE flank of the larger edifice, 3029-m-high Cuxliquel. The headwaters of the Río Samalá trace an arcuate path around the dome complex beginning on its SE side around to the north side and then to the SW. Thick Los Chocoyos pyroclastic-flow deposits from the eruption that formed Atitlán caldera to the SE fill much of the basin and extend down the Río Samalá to the SW.

San Pedro
Volcán San Pedro is the oldest of three 3000-m-high stratovolcanoes constructed within the roughly 85,000-year-old Atitlán III caldera. The 3020-m-high San Pedro forms a forested cone that rises above the SW side of scenic Lake Atitlán. Santiago bay, a narrow 8-km-long inlet of Lake Atitlán, separates the eastern flank of San Pedro volcano from the slopes of Volcán Tolimán. The shallow summit crater of San Pedro is breached to the NW and partially filled by a low mound of lava. Two cinder cones were constructed on the floor of the moat between San Pedro and the SW wall of Atitlán caldera. The age of the most recent activity of San Pedro is unknown, although the volcano is more vegetated and erosionally modified than the twin volcanoes of Tolimán and Atitlán and does not display evidence of fumarolic activity.

Barahona
The silicic Barahona caldera complex, which lies NE of Acatenango volcano and NW of Agua volcano, consists of two overlapping calderas. The northern caldera is 4.5 km in diameter and its floor is the site of the town of Santa Catarina Barahona, after which the complex is named. The southern caldera is about 2 km in diameter. The initial eruptions of the Barahona complex produced the Sumpango group of tephras, which date back to 300,000-250,000 years. The youngest tephra from Barahona is less than 23,000 years old. The rhyolitic and rhyodacitic tephras include 5 plinian deposits and a pyroclastic-flow deposit.

Piedra Grande
A cluster of faulted, heavily eroded andesitic stratovolcanoes is located in the Tecuamburro graben, between the Jalpatagua fault and Tecuamburro volcano. The vent area of Piedra Grande, on the north, lies with 4-km-wide, nested depressions open to the east. Much of the upper part of the andesitic volcano is extensively hydrothermally altered, and a fumarole is present. To the south is El Sordo, a basaltic-andesite stratovolcano with a smaller depression breached to the ESE. One lava flow has a Potassium-Argon age of 1.180 +/- 0.080 million years (Ma). To the south the Piedra Grande complex interfingers with El Sordo, an eroded and faulted basaltic cone. To the SW is Los Sitios, a sequence of interfingering andesitic lava flows from two eroded and faulted scoria and cinder cones. One flow has a Potassium-Argon age of 0.800 +/- 0.061 Ma.

Pueblo Nuevo Viñas
The deeply dissected Pueblo Nuevo Viñas (also known as Cerro la Gabia) is located between Pacaya and Tecuamburro volcanoes. The andesitic-dacitic stratovolcano has undergone edifice collapse that left a large horseshoe-shaped caldera breached to the NE and a debris-avalanche deposit that is overlain by the village of Pueblo Nuevo Viñas. Four cinder cones are located on the NE flank, and lava flows cover the western portion of the Cuilapa quadrangle. A Potassium-Argon age of 2.6 +/- 0.3 million years (Ma) was obtained from an older volcano in the complex, and an age of 0.821 +/- 0.118 Ma from a younger stratovolcano (Duffield et al., 1991).

Ixhuatan
The low-angle, eroded Ixhuatán volcanic complex covers a broad area between Tecuamburro and Moyuta volcanoes, south of the major regional Jalpatagua fault. The dominantly andesitic volcano was assigned a Pliocene-Pleistocene age by Reynolds (1987), and a Potassium-Argon date of 1.160 +/- 0.050 million years was obtained by Duffield et al. (1989) on a lava flow. Silicic pyroclastic-flow deposits are found in the Río los Esclavos, west of the volcano. The youngest center is a dacitic lava-dome complex at Cerro los Achiotes. The domes and associated ashfall and ashflow deposits partially fill and extend from a horseshoe-shaped caldera that is breached to the SE and may have formed as a result of slope failure. A N-S-trending fault zone that cuts across the volcano was the site of a seismic swarm in 1979-80.

Ayarza
Ayarza is a double caldera that lies about 40 km NE of the active Guatemalan volcanic front. The 5 x 7 km wide figure-8-shaped caldera is filled by the scenic Laguna de Ayarza, which is about 4 km wide in the western caldera and 2 km wide in the eastern caldera. Both calderas, whose steep walls rise nearly 600 m above the lake surface, were formed within several thousand years of each other during major rhyolitic explosive eruptions in the late Pleistocene. The older eastern caldera was associated with eruption of the Mixta pumice fall and ashflow, which were radiocarbon dated at about 27,000 +/- 1600 years before present (BP). The larger western caldera was formed during eruption of the Pinos Altos airfall pumice and Tapalapa ashflows radiocarbon dated at 23,100 +/- 500 years BP. Formation of the double caldera appears to be the last volcanic activity at Ayarza; bathymetry of the lake floor does not show evidence for post-caldera eruptions.

Cerro Alutate
Cerro Alutate is a small Quaternary stratovolcano located well north of the Guatemalan volcanic front, about 20 km north of Lake Ayarza. It is part of the so called Behind-Volcanic-Front region (Walker, 1981; Libbey et al., 2015). Other areas of Quaternary volcanics are found to the NW and NE in a region of mostly Tertiary volcanic rocks, south of the Motagua fault system.

Jumay Volcanic Field
Jumay stratovolcano rises 700 m above the city of Jalapa, just south of the boundary with folded Paleozoic low-grade metamorphic rocks. A shallow crater is located at the summit of the 2174-m-high volcano, which lies at the NE end of the broad area of Quaternary volcanic rocks in SE Guatemala. Widespread basaltic lava flows occur on the NW flank of the volcano. The age of the Quaternary volcano is not known precisely.

Cerro Ananopa
Cerro Ananopa is a Quaternary basaltic lava cone and lava flow on the floor of the Río Motagua valley, WSW of the town of El Jicaro. Scattered basaltic lava flows occur nearby, mostly south of the Río Motagua, and several Quaternary rhyolitic lava flows were mapped north of the river. These are part of a series of Quaternary volcanic rocks erupted through Paleozoic-to-Mesozoic metamorphic rocks parallel to the major WSW-ENE-trending Motagua fault system, which cuts both sides of the Río Motagua valley.

Guistepeque Volcanic Field
Güistepeque volcanic field consists of a cluster of Quaternary cinder cones and lava cones north of Suchitán volcano. The basaltic cones are located within the N-S-trending Ipala graben, and several of the cones were consequently constructed along N-S-trending fissures within the graben.

Cerro Redondo
Cerro Redondo is the central feature of a Quaternary volcanic field immediately west of Lake Guija near the border with El Salvador. Two overlapping basaltic shield volcanoes were constructed along a N-S line west of the lake. Small lava fields, capped by cinder cones and small lava domes, are located east, west, and NE of the shield volcanoes. Unlike in other volcanic fields in SE Guatemala, many of the cones in this area show random orientations unrelated to regional trends.

Conchagua
El Salvador and Honduras
Conchagua (also known as Cochague) is a conical edifice consisting of two overlapping stratovolcanoes, Ocotal and Banderas, overlooking the Gulf of Fonseca at the SE tip of El Salvador. It is elongated WSW-ENE, and the eastern and southern flanks descend into the sea. Cerro de La Banderas has a large horseshoe-shaped crater open to the NE, and though it appears younger, Ar-Ar dating by Quezada and Garcia (2008) was 0.41 +/- 0.1 Ma. To the WSW, the slightly higher Cerro del Ocotal, at 1225 m, was dated at 0.15 +/- 0.02 Ma. Ocotal has multiple peaks and the flanks are more dissected. Eruptions reported for the years 1522, 1688, 1868, 1892, and 1947 are erroneous, and may refer to landslides associated with earthquakes, an interpretation supported by Rapprich et al. (2010).

Conchaguita
El Salvador and Honduras
Conchagüita volcano occupies a small, 4-km-wide island in the Gulf of Fonseca across a narrow strait from Conchagua volcano. Late-stage eruptions formed a small, sharp-topped cone with a 100-m-wide summit crater at the southern end of the low 505-m-high island, and a youthful peninsula also extends from the island's eastern side. A crescent-shaped crater open to the west is located at the northern end of the island.

Masahuat Volcanic Field
El Salvador and Honduras
Cerro Masahuat is an eroded Pleistocene stratovolcano that lies at the NW corner of a major bend in the Río Lempa SE of Lake Guija. The Río Lempa surrounds Cerro Masahuat on all but the SE side and has cut a gorge through volcanic rocks of similar age to Masahuat that cover a broad area across the river to the north, east of Lake Guija.

Cerro las Tablas
Cerro las Tablas, also known as Cerro la Gloria or El Amate, consists of two low overlapping stratovolcanoes of Pleistocene age located at the SW corner of a major bend of the Río Lempa, NE of Coatepeque caldera. This Cerro las Tablas, distinct from the Cerro las Tablas of the Cerro Singüil volcanic field, lies at the SW end of a chain of Pleistocene volcanoes extending to the NE that includes Cerro las Visiones, Cerro Pacho, and Cerro Agua Helada.

Los Limones Volcanic Field
Los Limones volcanic field consists of a group of five cinder and lava cones of Pleistocene age located near the Río Lempa north of Guazapa volcano.

Cerro Lolotique
A broad area of Quaternary volcanic rocks surrounds the town of Nueva Guadalupe, north and NW of Chinameca volcano. Loma Larga and Cerro Lolotique form west- and south-facing escarpments, respectively, that overlook Nueva Guadalupe and the town of Chinameca. Although the Pan-American highway traverses the flanks of the two escarpments, geologic studies have focused on the more dramatic neighboring volcanoes of the San Miguel-Tecapa cluster, and relatively little is known of the geologic history of this area.

Cerro Yayantique
Located about 11 km E of the Laguna Aramuaca maar, Cerro Yayantique is the most prominent and least-eroded feature in a broad area of Pleistocene volcanic rocks in the SE corner of El Salvador west of the NW arm of the Gulf of Fonseca. Mapped as Pliocene by Weber and Wiesemann (1978).

A broad area of isolated small volcanic cones of Pleistocene age is located in eastern El Salvador near the border with Honduras, west of the Río Goascoran and north of the city of Santa Rosa de Lima.

Cerro Cacahuatique
Cerro Cacahuatique is a massive Pleistocene stratovolcano located in the interior valley of El Salvador about 30 km NNE of San Miguel volcano. The volcano (also spelled Cerro Cacaguatique) rises 1000 m above its base and is deeply dissected, although it still retains its subdued conical form. A large erosional caldera, formed through a breach on the SE side, truncates the summit.

Cerro Buena Vista
Cerro Buena Vista is an eroded Pleistocene stratovolcano located in the Jucuarán Range in the SE corner of El Salvador. The 750-m-high volcano lies near the Pacific coast, SW of Laguna de Olomega. A broad crater roughly 1 km wide is breached to the WSW.

Isla Zacatillo
Isla Zacatillo lies only 2 km off the eastern tip of El Salvador in the Gulf of Fonseca. The low, roughly 3-km-wide island is crudely rectangular in shape, but has a peninsula extending to the NE. A steep escarpment truncates the western side of the island below its summit. NNW-SSE-trending faults cut lava flows on the island. The smaller nearby island of Martín Pérez to the SE is also of Pleistocene age.

Isla Meanguera
Isla Meanguera, located in the Gulf of Fonseca SE of Conchagüita Island, consists of an elongated line of three small stratovolcanoes of Pleistocene age. A N-S-trending graben cuts the summits of all three volcanoes. A circular crater occupies the summit of the central cone, which forms the island's high point at 493 m.

Montaña de Izopo
Montaña de Izopo, a small basaltic shield volcano located about 20 km SE of the capital city of Tegucigalpa, is the highest Quaternary volcano in Honduras. The 2020-m-high volcano rises only 200 m above its base and was constructed along a NE-trending line parallel to the high fault scarps bordering the Zamorano valley. More extensive basaltic lavas were erupted at Santa Elena along this same NE-trending line. Other basaltic lava flows were erupted farther to the NE near Joya Grande and from other parallel NE-trending faults to the east.

Cerro de Hule
A broad, low-angle shield volcano located about 16 km south of the capital city of Tegucigalpa, Cerro de Hule is the second most prominent Quaternary volcano of the central Honduran plateau. Cerro de Hule was constructed at the intersection of two fracture systems and fed basaltic lava flows in all directions. The longest lava flow traveled 10 km to the NE and is now traversed over much of its length by the Carretera del Sur highway.

Cerro Gavilantepeque
Cerro Gavilantepeque is a small Quaternary basaltic shield volcano located about 10 km SSE of Tegucigalpa. Small remnants of lava flows cap adjacent mesas.

El Pedregal
El Pedregal, the most prominent Quaternary volcano in the highlands of central Honduras, is a low-angle basaltic shield volcano constructed on a high plateau of Miocene ignimbrites immediately west of the capital city of Tegucigalpa. A small ephemeral pond occupies a saucer-shaped summit depression. Isolated remnants of basaltic lava flows from El Pedregal and separate vents occur over broad areas primarily to the west, but NW nearly to the village of Zambrano. A small cone near Matasano produced reddish scoria during the only pyroclastic eruption in the Quaternary volcanic fields near Tegucigalpa.

Cerro Calanterique
Lava cone
Cerro Calanterique, located 1.5 km NW of the town of Siguatepeque, SE of Lake Yojoa, is the apparent source of an outcrop of Quaternary basaltic lava on the flat valley floor about 1.5 km west of town.

Maderas
Nicaragua
Volcán Maderas is a roughly conical stratovolcano that forms the SE end of the dumbbell-shaped Ometepe island in Lake Nicaragua. The basaltic-to-trachydacitic edifice is cut by numerous faults and grabens, the largest of which is a NW-SE-oriented graben that cuts the summit and has at least 140 m of vertical displacement. The small Laguna de Maderas lake occupies the bottom of the 800-m-wide summit crater, which is located at the western side of the central graben. The SW side of the edifice has been affected by large-scale slumping. Several pyroclastic cones, some of which may have originated from littoral explosions produced by lava flow entry into Lake Nicaragua, are situated on the lower NE flank down to the level of Lake Nicaragua. The latest period of major growth was considered to have taken place more than 3000 years ago, but later detailed mapping has shown that the most recent dated eruptive activity took place about 70,000 years ago and that it has likely been inactive for tens of thousands of years (Kapelanczyk et al., 2012). A lahar in September 1996 killed six people in an E-flank village, but associated volcanic activity was not confirmed.

Malpaisillo
Nicaragua
Pyroclastic shield
A large but topographically indistinct pyroclastic shield volcano lies in the Nicaraguan depression at Malpaisillo, NE of Las Pilas volcano and NNW of Momotombo volcano. The 10-km-wide Malpaisillo caldera, also known as Cerro el Chúcaro, forms a flat plain on the floor of the graben that contrasts dramatically with surrounding extensively dissected dacitic airfall and ignimbrite deposits. These deposits extend across the graben east of the Marrabios Range and reach into Lake Managua to the SE. They also crop out west and south of the Marrabios Range. A K-Ar age of 0.46 million years was obtained from the Malpaisillo deposit.

Apoyo
Nicaragua
The scenic 7-km-wide, lake-filled Apoyo caldera is a large silicic volcanic center immediately SE of Masaya caldera. The surface of Laguna de Apoyo lies only 78 m above sea level; the steep caldera walls rise about 100 m to the eastern rim and up to 500 m to the western rim. An early shield volcano constructed of basaltic-to-andesitic lava flows and small rhyodacitic lava domes collapsed following two major dacitic explosive eruptions. The caldera-forming eruptions have been radiocarbon dated between about 21,000-25,000 years before present. Post-caldera ring-fracture eruptions of uncertain age produced lava flows below the scalloped caldera rim. The slightly arcuate, N-S-trending La Joya fracture system that cuts the eastern flank of the caldera only 2 km east of the caldera rim is a younger regional fissure system structurally unrelated to Apoyo caldera.

Cerro San Jacinto
Cerro San Jacinto, also known as Cerro San Jacinto Viejo, is a small stratovolcano constructed along the eastern margin of the Nicaraguan central graben east of Lake Managua. A large central depression is surrounded on the north and east by a horseshoe-shaped ridge, which is a remnant of a caldera rim. San Jacinto was considered to be of possible Holocene age on the basis of youthful morphology (McBirney and Williams, 1965). However, the volcano is highly dissected relative to the Holocene volcanoes across the Nicaraguan depression to the west. Van Wyk de Vries (1999 pers. comm.) noted that the volcano is substantially older than nearby Las Lajas volcano and is of probable early Pleistocene age.

Tambor Grande
The eroded Tambor Grande caldera is one of several areas of Quaternary volcanic rocks along the Atlantic coastal plain at the SE tip of Nicaragua shown on the geologic map of Nicaragua (INETER, 1995). The two largest areas are located WNW of the coastal city of San Juan del Norte near the headwaters of the Río Chiripa and WSW of San Juan del Norte, north of the Río San Juan. Tambor Grande has an easily recognized central caldera and radially eroded flanks. It lies within an area of dense rain forest with some 3000 mm annual precipitation. Several small cones lie south of Rama, near the Escondido River. Considering their well preserved morphology and the heavy rainfall in the Caribbean lowlands of Nicaragua, these structures can be considered to be Pleistocene in age (Incer 2005, pers. comm.). Quaternary basaltic volcanoes are also located along the Atlantic coastal plain across the border in Costa Rica.

Cerro Chopo
Costa Rica
The small pyroclastic cone Cerro Chopo (also known by the religious names of Anunciación, Coronación, or Asunción) lies south of the main Guanacaste Range and north of the city of Canas. The 250-m-high basaltic pyroclastic cone was constructed over regional ignimbrites and andesitic lava flows. The crater is oriented to the NW and was the source of olivine-basaltic lava flows. Cerro Chopo was roughly estimated by Alvarado (2000) to be of late Pleistocene age (perhaps 40,000-10,000 years old). The interior of the cone, which lies along the well-traveled road from Canas to Tilarán, has been exposed by quarrying for road construction materials. Another small isolated cinder cone of similar age, Corobici, lies along the Río Corobici to the west.

Cerro Tilaran
Costa Rica
Cerro Tilarán, also known as Cerro Tovar, is a small andesitic shield volcano that lies at the NW end of the Tilarán Range west of Lake Arenal. The 634-m-high Tilarán volcano rises immediately SW of the town of the same name. The morphologically youthful Tilarán cone is overlain only by tephra deposits from Arenal (maximum age about 7000 years), however an Ar-Ar date of 1 million years was obtained (Alvarado, 2000) and the volcano is of Pleistocene age (Alvarado 2005, pers. comm.). The Tilarán Range, which lies to the west of the main volcanic chain, is a fault-bounded tectonic block of Miocene-Pleistocene andesitic rocks of the Monteverde formation. The densely forested range is renowned for its abundant exotic birds and wildlife.

Los Perdidos
Costa Rica
The forested Los Perdidos volcano lies at the southern end of a NNW-SSE-trending volcanic chain that includes the Arenal-Chato complex across the Río Fortuna. Volcanism began during the late Pleistocene at Los Perdidos and migrated northward to the historically active Arenal volcano. Several andesitic lava domes were constructed within and on the rim of a caldera, which have been have been Potassium-Argon dated by Gillot et al. (1994) at about 83,000-99,000 years before present.

Laguna Poco Sol
Explosion crater(?)
Laguna Poco Sol is a 200-m-wide, lake-filled depression that lies near the southern end of a volcanic lineament extending northward to Arenal volcano. The lake has been interpreted as a phreatic explosion crater or possibly a depression associated with a landslide. Lava flows, lahar deposits, tuffs, and volcanic breccias are found near the lake. Thermal activity at the lake and near the Río Penas Blancas includes mud pots, hot springs, and sulfur deposition.

Cerro San Miguel
Cerro San Miguel is an isolated lava dome that was constructed on the SW flank of the Tilarán Range near the mouth of the Gulf of Nicoya, NE of the port city of Puntarenas. The dacitic dome covers an area of about 9 km2 and was Potassium-Argon dated at less than 700,000 BP. A series of vertical-to-subvertical concentric fractures cuts the upper part of the dome.

Cerro las Mercedes
Cerro las Mercedes (also known as Cono Mercedes) is a cinder cone of late-Pleistocene age that lies along the Caribbean coastal plain near the border with Nicaragua. The cone lies just west of the Río San Juan near the point where the Costa Rica-Nicaragua border no longer follows the Río San Juan and extends westward south of the river. Leucite-bearing bombs and lapilli of potassic alkaline basaltic composition cover an area of about 1 km2.

Cerro Negro
The low Cerro Negro lava shield occupies an isolated position in the center of the Caribbean coastal plain immediately west of the Río Chirripó 17 km ENE of the town of Puerto Viejo. Lava flows in the area near this small 136-m-high shield volcano have been dated at from about 24 million years to about 1 million years (Alvarado 2005, pers. comm.).

Lomas de Colorado
Five small Pleistocene shield volcanoes located along the Ríos Colorado and Chirripó form the Lomas de Colorado volcanic field. This group of small alkaline basaltic volcanoes is located near the Caribbean coastline at the NE-most corner of Costa Rica and covers an area of about 50 km2. The highest peak, Cerro Cocorí, is 7 km S of the confluence of the Río Chirripó and the Río Colorado. A lava flow from one of three shields named Cerro Coronel was Potassium-Argon dated at 1.2 million years (Bellon and Tournon, 1978). The westernmost part of the Lomas de Colorado is a hill known locally as Chirripó Atlántico, lying west of the Cocorí lava shield and east of the lengthy north-flowing portion of the Río Chirripó.

Tortuguero
Tortuguero is a Pleistocene pyroclastic cone on the Atlantic coastal plain adjacent to the Caribbean Sea (Barquero and Saenz, 1987; Alvarado, 2000). The small 119-m-high basaltic pyroclastic cone was constructed over fluvial sediments along one of the many coastal lagoons common in this part of the Carribean coastline. The cone lies near the northern boundary of scenic Tortuguero National Park, a popular coastal rainforest park rich in birds and wildlife.

Lomas de Sierpe
The Lomas de Sierpe, also known as Cerro Las Lomas Azules, are a group of six small Pleistocene shield volcanoes (Barquero and Saenz, 1987; Alvarado, 2000) on the Caribbean coastal plain between the Tortuguero and Parisimina rivers. The highest of the small shield volcanoes, which cover an area of about 70 km2, is Colon. Some of the volcanoes lie within Tortuguero National Park, known for its abundant birds and wildlife, turtle nesting areas, and rain-forest-lined canals known as Costa Rica's Amazon.

Durika
A group of Pliocene-Pleistocene dacitic lava domes, the Dúrika volcanic field (also known as the Río Lori domes), lies in the Talamanca Range of eastern Costa Rica. A Potassium-Argon date of 0.9 million years was obtained from one of the domes (de Boer et al., 1995). The domes lie on the NE side of the crest of the Talamanca Range near the headwaters of the Río Lori, a tributary of the Río Coen.

Isla del Coco
The 22 km2 rain-drenched Isla del Coco (Cocos Island) lies astride the central part of the aseismic Cocos Ridge about 650 km SW of the Costa Rican port of Puntarenas. It is the only subaerial portion of the Cocos Ridge, which extends from the Galápagos hot spot to the Mesoamerican trench. The island was discovered by the Spanish pilot Juan Cabeas in about 1526 and is renowned as the site of treasures buried by pirates and ship captains. The roughly rectangular 5 x 7 km island is surrounded on all sides by steep cliffs up to 200 m high. Construction of a Pliocene-Pleistocene shield volcano was followed by caldera formation and the emplacement of a trachytic lava dome. The latest eruptions produced lava flows that originated from NE-trending fissures most prominent on the SW part of the island.

Tisingal
Panama
Volcán Tisingal (also known as Cerro Colorado or Cerro Pecón) lies adjacent to the Costa Rica border in the Talamanca Range of westernmost Panama, NW of Volcán Barú. A large andesitic-dacitic stratovolcano was breached to the SW by edifice collapse, leaving a 7-km-wide horseshoe-shaped caldera. Cerro Picacho, on the NE rim of the caldera, forms the 2986 m high point of the volcano. Two large lava domes, andesitic Cerro Totuma and dacitic Cerro Pelón, were formed in the NW and E sides of the caldera, respectively. Two additional domes, the larger of which is Cerro Pando, lie outside the caldera to the SSW, and another dome, Cerro Punta, is east of the caldera. Potassium-Argon ages for the Volcán Colorado complex range from 1.66 million years to 0.52 million years.

La Yeguada
Panama
La Yeguada, also known as Chitra-Calobre, is a massive volcanic complex in west-central Panamá north of the Azuero Peninsula that was active from the Miocene into the Quaternary. The youngest major feature of La Yeguada is located within a large fault-bounded horst that forms the high point of the volcanic complex east of Laguna La Yeguada. The latest eruptions took place from the northern part of the horst about 220,000 years ago at Cerro Corero lava dome (also known as Cerro de la Charca), north of El Castillo. The youngest feature of the La Yeguada complex is the Media Luna cinder cone, which was erupted through Tertiary ignimbrite deposits at the NW side of the complex. The oldest peat layer within a small lake dammed by a basaltic lava flow originating from the cone was radiocarbon dated at about 300-350 years ago, but later dating has shown that flow was erupted about 45,000 years ago, and that the La Yeguada complex has not had Holocene eruptions. Warm springs are scattered throughout the complex, and the Chitra-Calobre geothermal field is one of three areas in Panamá that have been the object of intensive geothermal exploration.

Santa Rosa
Colombia
Eroded Pleistocene andesitic shield volcano (Herd 1982). Deposits from near the base of the volcano were dated as 2.3 ± 0.1 Ma (K-Ar whole rock) according to Thouret (1989).

Nevado del Quindio
Colombia
Nevado del Quindío is a Pleistocene stratovolcano located south of Santa Isabel volcano and NW of Nevado del Tolima volcano. The vent area is eroded by glaciers (Herd 1982).

San Augustín-Isnos
Colombia
A back-arc volcanic field with many pyroclastic cones lies in the Department of Huila, near the towns of San Augustín and Isnos, overlies an ignimbrite plain. Disappearance of the San Augustín culture between the 2nd century BCE and the first century CE has been attributed to invading armies or volcanic activity (Borrero et al., 2007).

Cutanga
Included in Latter Quaternary volcano list-no further information.

Animas
Las Animas is located about 11 km NE of Dona Juana volcano and 12 km SW of Petacas volcano, according to the Pasto Observatory. Included in Latter Quaternary volcano list.

A back-arc volcanic field in the La Plata and La Argentina area of the Department of Huila contains the small Meremberg stratovolcano and its 1.5-km-wide caldera and several pyroclastic cones, including the freshly preserved El Morro (Borrero and Castillo, 2006).

San Diego
Maar
Although the San Diego maar has been known and previously described by Servicio Geologico Colombiana, along with age dating by Toro (1988) that placed the most recent activity in the late Pleistocene-early Holocene, more recent work by Borrero et al. (2016) provides a more comprehensive understanding of this volcano. The NNE-elongated crater is about 1.5 x 2.1 km in size and contains a lake about 230 m below the crater rim. A cone feature located immediately NE of the maar is the remains of a dacitic dome with landslides on the flanks. They determined that the volcanic features were all the result of a single monogenetic eruptive period that began with the vent opening and incremental growth of the original crater, followed by additional widening of the maar. Effusion of the dome was the last stage of active volcanism. A paleosol below the young maar sequence was C14 dated at 20,056 ± 93 years cal BP, and the dome was slightly younger at 18 ka BP based on fission track dating of apatite.

El Escondido
Identified by the Servicio Geologico Colombiano in a press release in February 2015, this area of a partially collapsed crater and lava domes is covered in thick vegetation. SGC scientists tentatively estimated that the last eruption was 30 ka, but noted that there are hot springs in the area.

Chalpatan
Ecuador
The Chalpatan caldera is of Plio-Pleistocene age (Beate 1992, pers. comm.). A single Potassium-Argon age of 2.0 million years ago has been obtained (INECEL 1987).

Chiltazon
Ecuador
Pleistocene stratovolcano (Beate 1992, pers. comm.)

Iguan
Ecuador
Iguan is a Pleistocene stratovolcano with an avalanche caldera open to the WNW (Beate 1992, pers. comm.).

Yanaurcu de Pinan
Yanaurcu de Piñán is a stratovolcano of Pleistocene age (Beate 1992, pers. comm.).

Pilavo
Pilavo is Pleistocene stratovolcano (Beate 1992, pers. comm.).

Cotacachi
The steep-sided Pleistocene stratovolcano Cotacachi rises above Cuicocha caldera to the south.

Cusin
Cusín is a Pleistocene stratovolcano with a caldera open to the NW (Beate 1992, pers. comm.).

Casitagua
Casitagua is a Pleistocene stratovolcano with a caldera containing lava domes SW of Pululagua volcano (Beate 1992, pers. comm.).

Pambamarca
Pambamarca is a Pleistocene stratovolcano with two lava domes on the SE flank (Beate 1992, pers. comm.).

Pasochoa
Pasochoa is a Pleistocene stratovolcano with an avalanche caldera open to the NW (Beate 1992, pers. comm.).

Cerro Puntas
Cerro Puntas is a Pleistocene stratovolcano with an avalanche caldera open to the west (Beate 1992, pers. comm.).

Ilalo
Ilaló is a low, eroded Pleistocene stratovolcano immediately SE of Quito. A single Potassium-Argon age of 1.62 +/- 0.16 million years ago has been obtained (INECEL 1980).

Pan de Azucar
Pan de Azúcar is a large, probably alkalic volcano in the jungle NNW of Sumaco volcano and east of the town of Baeza. The 3482-m-high volcano was only relatively recently discovered on satellite images and was considered to be Holocene in age because it is otherwise not likely to be so well preserved in a region with heavy rainfall (Hall 1987, pers. comm.). Later work suggested that the volcano was substantially older than neighboring Sumaco volcano and was of probable late-Pleistocene age (Eissen, 2006, pers. comm.).

Santa Cruz
Santa Cruz is a small stratovolcano of Pleistocene age with a caldera open to the north (Beate 1992, pers. comm.).

Sincholagua
Sicholagua is an eroded Pleistocene volcano NNE of Cotopaxi volcano (Beate 1992, pers. comm.).

Ruminahui
Rumiñahui is a Pliocene or Pleistocene stratovolcano with a summit caldera NE of Cotopaxi volcano (Hall 1987, pers. comm.).

Corazon
Corazón is an early to mid Pleistocene stratovolcano with a summit caldera (Hall 1977). Late Pleistocene lavas are also present.

Chalupas
The 18-km-wide Pleistocene Chalupas caldera is the source of the about 90 km3 Chalupas ignimbrite, the largest known in the northern Andes during the Quaternary (Beate, 1989). The Pleistocene Quilindana stratovolcano is located within the caldera. The youngest intracaldera lava flow are unaffected by glaciation.

Putzalagua
Putzalagua is a Pleistocene lava dome near Latacunga (Hall 1987, pers. comm.).

Sagoatoa
Sagoatoa is an eroded Pleistocene stratovolcano with flank cones (Beate 1992, pers. comm.).

Igualata
Igualata is an eroded Pleistocene stratovolcano between Chimborazo and Tungurahua volcanoes (Hall 1987, pers. comm.).

Llimpi
Llimpi is a small late Pleistocene stratovolcano NE of Tungurahua volcano (Hall 1987, pers. comm.).

Puyo
A series of 9 scoria cones NE of Puyo are aligned along a NW-SE fissure. A 40Ar-39Ar date of 190 +/- 7 ka was obtained by Hoffer et al. (2008).

Carihuairazo
Carihuairazo is an eroded Pleistocene stratovolcano truncated by edifice collapse, leaving a caldera breached to the NE. A younger volcano, Puñalica, was constructed between about 18,000 and 14,000 years before present 5 km east of Carihuairazo (Clapperton 1990). A landslide and lahar in 1698 produced debris that reached the town of Ambato (Hall 1987, pers. comm.).

Calpi
Tuff cone(s)
A group of tuff cones and lava flows of Pleistocene age is located SW of Chimborazo volcano (Beate 1992, pers. comm.).

Altar
Altar is a large stratovolcano of Plio-Pleistocene age with a caldera breached to the west (Hall 1987, pers. comm.). Indian legends report that the top of Altar collapsed after seven years of activity in about 1460, but the caldera is considered to be older than this (Catalog of Active Volcanoes of the World, Hall, 1977).

Roca Redonda
Galapagos Islands
The tiny flat-topped islet of Roca Redonda, only 50 x 100 m wide, is the remnant of a large shield volcano north of Isabela Island. Shallow submarine fumaroles are present around the island, and a single K-Ar date of essentially zero age (53 +/- 54 ka) was obtained.

Culpepper
Galapagos Islands
Culpepper Island (also known as Darwin Island) is a small flat-topped island encircled by cliffs that lies NE of the Galápagos platform. A single magnetic measurement indicates an age of <0.72 million years ago.

Wenman
Galapagos Islands
Wenman Island (also known as Wolf Island) and three nearby smaller islands are the eroded remnants of a shield volcano. The western part of the island and the small low western island may represent caldera-filling lava lake deposits. Remnant magnetism of two samples is reversed, indicating an age between 2.47 and 0.72 million years ago (Cox, 1983). A date of 1.6 +/- 0.07 million years was obtained from Wolf Island (Harpp and Geist, 2002).

Rabida
The most petrologically diverse of the Galápagos Islands, the small 2-km-wide Rábida Island consists of a group of lava domes and pyroclastic cones ranging in composition from tholeitic basalts to trachytes. Potassium-Argon dates from lava flows range from 1.06 to 0.l92 million years ago (Cox 1983).

Pinzon
The Pinzón Island shield volcano is covered with lava flows originating from a crater SW of the summit. The most prominent feature is a small steep-walled 1-km-wide caldera NW of the summit. Potassium-Argon dates range from 1.09 to 0.93 million years ago (Cox 1983).

Santa Fe
Santa Fe Island consists of the faulted remnant of a Pliocene shield volcano capped by numerous cinder cones. Potassium-Argon dates range from 3.9-0.72 million years ago (Geist et al., 1986; White et al., 1993). Fumarolic activity was observed in 1970, but not in 1984.

Floreana
The low shield volcano of Floreana Island, also known as Charles Island or Santa María Island, is densely covered with cinder cones. A 5-km-wide caldera at the center of the island has an irregular floor. Several young lava flows were considered to have been as young as few thousand or even a few centuries old based on their youthful morphology (McBirney and Williams, 1969), but a surface exposure age of 26 +/- 7 ka was obtained on the youngest flow (Kurz and Geist, 1999). An 1813 eruption attributed to Floreana in the Catalog of Active Volcanoes of the World is considered to have actually occurred at Sierra Negra volcano on Isabela Island (Simkin 1980, pers. comm.). The most conspicuous of the cinder cones on the island is Cerro de Pajas, which rises 335 m above its surroundings. It fed a massive pahoehoe lava flow, perhaps the youngest on Floreana, that reached the SW coast over a broad 6.5 km area.

Huambutillo-Rumicola
Peru
A K-Ar date of about 0.59 +/- 0.25 Ma was obtained from Huambutillo volcano at the eastern end of the Cuzco valley about 20 km SE of Cuzco. Nearby Rumicola volcano was dated at about 7.2 Ma, but this was considered to be in error, and the volcano to be of likely Quaternary age (Bonhomme et al., 1988).

Solimana
Peru

Nevados Firura
Peru
The Nevados Firura volcanic complex consists of a 10-12 km long, NE-SW-trending cluster of small stratovolcanoes. The highest peak is 5500-m-high Nevado Firura itself, which lies to the NE of Cerro Soncco Orcco and Cerro Jahsaya. Little is known about this andesitic volcanic complex, but morphologically youthful lava flows extend into vegetated and settled areas. The age of Nevados Firura was considered to be Holocene (de Silva and Francis, 1990), but later work showed that the young-looking lava flows on the flank of the volcano were dated at about several hundred thousand years (Worner 2006, pers. comm.).

Cerros Purupuruni
The Cerros Purupuruni are a group of lava domes of probable Pleistocene age (de Silva 2007, pers. comm.).

Ollague
Northern Chile, Bolivia and Argentina
Volcán Ollagüe, also known as Oyahué, is a massive andesitic stratovolcano with a summit dacitic lava dome. A large Pleistocene debris-avalanche deposit extending westward separates the Salar de San Martín from the Salar de Ollagüe. Three youthful-looking silicic lava flows mark late post-collapse eruptions, but show evidence of glaciation and are thought to pre-date the last glacial advance at about 11,000 years ago (Freeley et al., 1993). A youthful-looking scoria cone on the lower WSW flank, La Poruñita, was initially considered to be of Holocene age (González-Ferrán, 1995), however Wörner et al. (2000) later obtained Potassium-Argon dates of 420,000 to 680,000 years. Active sulfur mines on the upper western and southern flanks are reached by a road that climbs to about 5500 m elevation. No historical eruptions have been recorded; activity has been restricted to periods of intense fumarolic activity, and a persistent steam plume emanates from a fumarole on the south side of the summit dome.

Copiapo
Northern Chile, Bolivia and Argentina
Volcán Copiapó in Atacama province SW of Nevados Ojos del Salado volcano is a dominantly Miocene-Pliocene stratovolcano. Eight andesitic pyroclastic cones are located primarily on the SE flank of the 6052-m-high volcano. The most recent cone, Volcán San Román, lies 7 km north of Copiapó and was considered to be of probable Pleistocene age, related to late-stage reactivation of Pleistocene-Holocene fissures cutting the Ojos del Salado region (González-Ferrán, 1995). This dacitic-to-andesitic volcano was reported by Von Wolff (1929) to display solfataric activity.

Cerro Pucara
Northern Chile, Bolivia and Argentina
Cerro Pucara is a volcanic field with pyroclastic cones of Pleistocene age, with nearby ages of 1.0-0.6 million years (de Silva 2007, pers. comm.). The Pataca Kollu cones are considered part of this volcanic field.

Patilla Pata
The International Association of Volcanology and Chemistry of the Earth's Interior data sheets (1973) classified Patilla Pata volcano in Bolivia NW of Sajama volcano as being active during the past 2000 years, but de Silva (2007 pers. comm.) noted no evidence from analysis of satellite images for Holocene activity in this area. Patilla Pata has undergone extensive glacial erosion. The andesitic stratovolcano has also produced basaltic lava flows.

Nevado del Sajama
Nevado del Sajama, rising to 6542 m about 20 km E of the Chilean border, is Bolivia's highest mountain. The prominent glacier-clad edifice consists of an andesitic stratovolcano overlying andesitic-to-rhyodacitic lava domes. Sajama borders Volcán Cholcani on the SE, and flank centers occupy the saddle between the two peaks. The steep-sided volcano towers about 2200 m above its base, and glaciers descend to about 5600 m. The age of the most recent activity has variously been considered to be Holocene, Pleistocene-Holocene, or Pleistocene, but de Silva (2007 pers. comm.) noted no evidence of Holocene activity.

Volcan Larancagua
Volcán Larancagua is Plio-Pleistocene in age (Moreno, 1985).

Caquena
The Caquena andesitic lava domes are Potassium-Argon dated around 194,000 to 264,000 years before present (Worner et al. 1988).

Vilacollo
Lava flows from the Vilacollo cinder cones are Potassium-Argon dated around 285,000 years before present (Worner et al. 1988).

Acotango
Acotango, along with Volcán Humarata to the north and Cerro Capurata (also known as Cerro Elena Capurata) to the south, comprises the Nevados de Quimsachata volcano group. Quimsachata means "three" in the Andean Aymará language, and 5730-m-high Humarata, Acotango, and 5990-m-high Cerro Capurata straddle the Chile-Bolivia boundary along a roughly N-S line. The 6052-m-high Acotango stratovolcano is the central and highest of the three stratovolcanoes. It is in a fairly advanced stage of dissection, but a morphologically youthful lava flow on its northern flank suggested Holocene activity (de Silva and Francis, 1991). Later higher resolution imagery implied a Pleistocene age (de Silva 2007, pers. comm.). Humarata, with a summit crater breached to the ESE, and Capurata, a complex of lava domes and associated pyroclastic-flow deposits, may also have been active during the Holocene.

Lexone
The eroded Lexone volcano contains a group of young lava domes in northern Chile SE of Tacora volcano. The domes were initially considered from morphological evidence to be of Holocene age (Moreno 1985, pers. comm.), but K-Ar dates of about 60,000-70,000 years were obtained from the young chain of lava domes (Clavero 2004, pers. comm.).

Nevado Anallajsi
The International Association of Volcanology and Chemistry of the Earth's Interior data sheets (1973) listed Nevado Anallajsi volcano in Bolivia north of Sajama volcano as being active during the past 2000 years, but de Silva and Francis (1990) noted no evidence from analysis of satellite images for Holocene activity in this area. The andesitic-to-dacitic compound volcano overlies an ignimbrite plateau. Younger basaltic lava flows were erupted from a north-flank vent, but Woerner (2006 pers. comm.) indicated there was certainly no Holocene activity at Anallajsi.

Arintica
Volcán Arintica is the central and most prominent cone of a large volcanic complex that rises north of the Salar de Surire. The complex includes Cerro Puquintica (also called Poquentica), 7 km to the east, Cerro Calajata, 3 km to the SW, and the dacitic Calajata lava dome at the SW end of the complex. The volcanoes are extensively dissected, but the latest activity at 5597-m-high Arintica produced a postglacial lava flow from a relatively well-preserved summit crater that descended the SE flank (de Silva and Francis, 1991). Later higher-resolution imagery indicated this lava flow was a collapse deposit and the volcano had a probable Pleistocene age (de Silva 2007, pers. comm.). Potassium-Argon ages of 637,000 and 486,000 yrs were obtained by Wörner et al. (2000), who suggested that based on the elevation and location of the volcano, the summit may not have been glaciated and that consequently the lack of glaciation may not denote Holocene activity. Cerro Puquintica (Poquentica) is considerably older than Arintica and rises to 5760 m.

Rochaculla-Inca Camacha
These volcanoes display hydrothermal alteration (IAVCEI, 1973) and are of possible Pleistocene age (de Silva, 2007 pers. comm.).

Cerro Tatajachura
Cerro Tatajachura stratovolcano of Pliocene-Pleistocene age was the source of voluminous andesitic lava flows (Gonzalez-Ferran, 1995).

Cerro Cariquima
Cerro Cariquima is a youthful-looking stratovolcano, but could be Pliocene in age (Worner, 2006 pers. comm.) Similar appearing volcanoes elsewhere in this part of the Andes were K-Ar dated at about 3 million years. An unnamed cinder cone corresponding to the location of Cerro Pina on the lower NE flank was classified by IAVCEI (1973) as being active during the past 2000 years. Worner (2006 pers. comm.) however indicated there was no young volcanism in this area, and de Silva and Francis (1991) noted no evidence from satellite imagery of young volcanism here.

Porquesa
The massive Porquesa lava-dome complex produced small-volume ignimbrites dated at 0.15 and 0.29 million years ago (Worner et al., 2000).

Cerro Napa
Cerro Napa has a Potassium-Argon date of 1.38 million years (Worner et al., 2000).

Ocana
Pleistocene stratovolcano (Moreno 1985).

Cerro Copa
Pleistocene stratovolcanoes (Moreno 1985).

Aucanquilcha
The world's highest permanent human habitation is situated below a sulfur mine in the summit region of Cerro Aucanquilcha, one the largest volcanoes of northern Chile. Several distinct cones are located along a 10-km-long, E-W ridge that forms the broad summit. A Pleistocene debris-avalanche deposit is a prominent feature on the lower NW flank. Extensive Pleistocene glacial moraines surround the stratovolcano, but postglacial lava flows overlie these moraines on the upper southern flanks (de Silva and Francis, 1991). Wörner et al. (2000) obtained surprisingly old Potassium-Argon dates of 400,000 to 780,000 years from the youngest flows on the NE and SW flanks, and eruptive activity appears to have ended during the late Pleistocene. It presently displays fumarolic activity.

Cerro San Agustin
The International Association of Volcanology and Chemistry of the Earth's Interior data sheets (1973) considered the andesitic-to-dacitic Cerro San Agustín stratovolcano to have been active during the past 2000 years, but de Silva and Francis (1991) noted no evidence from analysis satellite images of Holocene activity in this area, and de Silva (2007 pers. comm) considered the volcano to be of Pleistocene age.

Escala
Endogenous extrusions at the andesitic Escala lava dome in SW Bolivia occurred during the Holocene (Kussmaul et al., 1977). Later analysis of higher-resolution satellite imagery showed no evidence of Holocene domes in this area (de Silva 2007, pers. comm.).

Cerro Moiro
The International Association of Volcanology and Chemistry of the Earth's Interior data sheets (1973) listed Cerro Moiro (also known as Cerro Negro) in SW Bolivia as being active during the past 2000 years, but de Silva and Francis (1991) found no evidence from satellite image analysis of Holocene activity. Later higher-resolution satellite imagery suggested a possible Pleistocene age (de Silva 2007, pers. comm.). The andesitic scoria cone was constructed on a rhyolitic ignimbrite plateau.

Cañapa
Cañapa is an andesitic-dacitic stratovolcano of Plio-Pleistocene age (Gonzalez-Ferran, 1995). De Silva (2007 pers. comm.) considered the volcano to be of Pleistocene age.

Cerro Ascotan
The orrect name is Ascotán (Moreno, 1985 pers. comm.), not Acostán (IAVCEI, 1973). De Silva (2007 pers. comm.) considered the volcano to be of Pleistocene age.

Paniri
Cerro Paniri is a complex stratovolcano located about 30 km SE of San Pedro volcano. The summit contains three craters separated by about 4 km along a NW-SE trend. The age of this andesitic-to-dacitic volcano was considered to be Pleistocene-Holocene (González-Ferrán, 1995), but de Silva (2007 pers. comm.) considered it to be of probable Pleistocene age.

Cerro del Leon
Cerro del León is an andesitic stratovolcano 40 km SE of the San Pedro-San Pablo volcanoes. It is flanked by two massive dacitic lava domes, 2.6 km3 Chillahuita to the SE and 26 km3 Chao to the NW, in the saddle between Cerro del Leon and Paniri volcanoes. González-Ferrán (1995) considered León to be of Pleistocene-Holocene age. The massive Chao lava dome and flow is the world's largest of its type. The 14.5-km-long dacitic lava flow has distal margins that are 350-400 m high and dramatic 30-m-high flow ridges on its surface. The age of the flows was considered to be post-glacial (Guest 1981, pers. comm.), but Argon-Argon dates indicate only that it is less than 100,000 years old (de Silva and Francis, 1991), and based on comparison with nearby dated flows, it was considered to be of Pleistocene age (de Silva, 2007 pers. comm.). The eruption of less than 1 km3 of dacitic pyroclastic flows preceded the initial lava extrusion, which formed the 22 km3 compound main flow. Eruption of a small amount of rhyolitic airfall and growth of a pumice cone was followed by effusion of the final 3 km3 of lava.

Deslinde
Quaternary (Guest 1969), not Holocene (Moreno 1985).

Volcan Linzor
Volcán Linzor is a 5680-m-high stratovolcano along the Chile/Boliva border. This andesitic volcano was considered to be Pleistocene-Holocene age by González-Ferrán (1995). De Silva (2007 pers. comm.) noted no evidence for Holocene activity at Linzor, which lies west of Laguna Colorada.

Jorcada
Volcán de Jorcada is an elongated fissure-controlled volcanic massif extending between the Pastos Grandes caldera and Laguna Colorada in Bolivia. More than 50 craters, small stratovolcanoes, and lava domes are located along four fissures covering an area of 230 km2. Eight small andesitic-to-dacitic stratovolcanoes with craters 0.2-1.5 km wide are located along the southernmost fissure. A second fissure, oriented NW-SE and 10 km long, contains ten volcanic centers with craters with widths of 0.2-1.2 km. A third fissure, trending NE, produced seven rhyodacitic lava domes. Activity has migrated to the north, with the youngest fissure, on the NW side of the complex, estimated to be of probable Holocene age (González-Ferrán, 1995). De Silva (2007 pers. comm.) dated this youngest fissure at 95,000 yrs BP. This NW-trending fissure, 7 km long, contains 27 small basaltic-andesite craters.

Quetena
Lava effusions along fissures at Quetena were considered to have occurred during the Holocene (Kussmaul et al., 1977). De Silva (2007 pers. comm.) indicated that volcanism in this area is pre-Holocene and may be Pleistocene or older.

Sunequera
Fernandez et al. (1973) noted that well-preserved craters favor activity in historical time, however de Silva (1990, pers. comm.) indicates that Sunequera is a pre-Holocene shield volcano with craters that are glacial cirques.

Uturuncu
Uturuncu, the highest peak of SW Bolivia, displays fumarolic activity, and postglacial lava flows were noted by Kussmaul et al. (1977). Inspection of satellite images of the 6008-m-high peak, located SE of Quetana, did not show evidence for postglacial activity (de Silva and Francis, 1991). Andesitic and dacitic lava flows dominate on Uturuncu, and no pyroclastic deposits were observed during recent field work. Although young lava flows display well-preserved flow features, youthful-looking summit lava flows showed evidence of glaciation. Two active sulfur-producing fumarole fields are located near the summit, and large-scale ground deformation was observed beginning in May 1992 (Pritchard and Simons, 2002), indicating, along with seismicity detected in 2009-10 (Jay et al., 2012), that a magmatic system is still present.

Cerro Chascon
The lava dome of Cerro Chascon and the associated rhyolitic Cerro Runtu Jarita lava flow are located within the moat of Bolivia's Pliocene Pastos Grandes caldera. The roughly circular, flat-topped Cerro Chascon is located immediately NW of Laguna Khara. Cerro Runtu Jarita forms a roughly N-S-trending chain of small silicic lava bodies that probably represents the surficial expression of a subsurface dike. Minor eruptions of rhyolitic tephra preceded extrusion of the Cerro Runtu Jarita lavas. The age of Cerro Chascon was considered to by Holocene (de Silva and Francis, 1991), but new K-Ar dates give ages of 0.88-0.93 Ma (Watts et al., 1999).

Apagado
Pleistocene stratovolcano (Moreno 1985).

El Volcan
El Volcán is one of several stratovolcanoes located east of the vigorous Geisers del Tatio geothermal field. Lava flows at the base of the volcano are dacitic, while those at the upper part are andesitic-to-dacitic. El Volcán was considered by González-Ferrán (1995) to be of Pleistocene-Holocene age, but de Silva (2007 pers. comm) assigned it a probable Pleistocene age.

Cerros de Tocorpuri
Cerros de Tocorpuri (or Volcán Tocorpuri) is a stratovolcano complex on the Chile-Bolivia border with a youthful-looking rhyolitic lava dome, Cerro la Torta, at its western foot. The international border swings around the eastern rim of a 1.4-km-wide crater that truncates the summit; the crater lies wholly within Chile. It was considered by González-Ferrán (1995) to be of Pleistocene-Holocene age. Cerro la Torta has been considered to be of Holocene age due to its youthful morphology, but its age is not known precisely and Potassium-Argon dating indicates only that it is less than a million years old. Comparison with similar dated domes nearby suggests it is of Pleistocene age (de Silva, 2007 pers. comm.). The circular, roughly 5 km3 Cerro la Torta was erupted from a central vent and is surrounded by a flat-topped surface with wrinkled flow ridges. The flow terminates in steep, talus-covered margins about 150 m high. Lava extrusion was preceded by minor silicic explosive eruptions.

Volcan Tatio
Quaternary (Guest and Sanchez, 1969); not Holocene (Moreno, 1985).

Poquis
Erupted on Pliocene ignimbrite plateau (IAVCEI). Upper Pleistocene (Moreno 1985).

Curutu
Upper Pleistocene (Moreno 1985).

Losloyo
Upper Pleistocene (Moreno 1985)

Potor
One of a group of upper Pleistocene volcanoes (Moreno 1985).

Hecar
stratovolcano north of Lascar volcano; no evidence for Holocene activity (de Silva and Francis 1991).

Laguna Verde
Laguna Verde is a 5464-m-high stratovolcano located west of Colachi volcano and is one of a cluster of young stratovolcanoes north and east of Lascar volcano. Laguna Verde volcano was considered to be of Pleistocene-Holocene age (González-Ferrán, 1995), but de Silva (2007 pers. comm.) indicated it was of probable Pleistocene age. The andesitic volcano, rising 1200 m above its base, collapsed to the north, producing a debris avalanche that dammed the Quebrada Portor, forming a lake.

Cerro de Rio Negro
Complex stratovolcano north of the Salar de Aguas Calientes; no evidence for Holocene activity (de Silva and Francis 1991).

Cerro Zapaleri
Cerro Polques is of probable Pliocene age, although some component could be Pleistocene (de Silva, 2007 pers. comm.).

Miscanti
Pleistocene (Moreno 1985).

Laco
Laco is a central dome surrounded by satellite craters, perhaps Pleistocene in age. Radiometric dates range from 2.17 to 1.8 million years (de Silva, 2007 pers. comm.).

Incaguasi
Pleistocene (Moreno 1985)

Capur
Pleistocene stratovolcano (Moreno 1985).

Aguas Delgadas
Aguas Delgadas volcano is listed as active during the past 2000 years (IAVCEI 1973), but no Holocene volcanoes are listed in this area by de Silva and Francis (1990). The volcanoes Cerro Bayo and Corrida de Cori, very near to the listed location of Aguas Delgadas, are classified as Pleistocene.

Tumisa
Potassium-Argon dates 1.2 to <0.4 Ma (Gonzalez-Ferran, 1995).

Lejia
Pleistocene (Moreno 1985).

Piedra Parada
Piedra Parada is a large stratovolcano with summit craters and lava flows that retain integrity in the upper part of the edifice and is of likely Pleistocene age (de Silva, 2007 pers. comm.).

San Francisco
San Francisco volcano has K-Ar dates of 1.34 and 1.32 million years ago (Gonzalez-Ferran, 1995).

Cerro de la Niebla
Cerro de la Niebla is a compound volcano of possible Pleistocene age (de Silva, 2007 pers. comm.).

El Azufre
El Azufre has a somewhat youthful morphology and could be of Pleistocene age (de Silva, 2007 pers. comm.).

Tres Cruces
The massive Tres Cruces complex of Pliocene-Pleistocene age covers an area of about 1000 km2 along the Chile-Argentina border (Gonzalez-Ferran, 1995). The Indio lava dome on the SW side of the complex was K-Ar dated at about 0.35 million years.

Los Patos
Los Patos is a large eroded stratovolcano of possible Pleistocene age (de Silva, 2007 pers. comm.).

Nevado Queva
Late-Quaternary flows with no radiometric age date (Hormann et al., 1973). De Silva (2007, pers. comm.) assigned a likely Pleistocene age.

Tocomar
The Tocomar volcanic center was the source of two major phreatomagmatic and phreatic eruptions during the Pleistocene. The Tocomar Ignimbrite of rhyolitic composition covers an area of 50 km2. It is located along the Calama-Olacapato-Toro fault zone south of Tuzgle and NE of Nevado Queva volcanoes.

Gemelos-Saladillo
The late-Pleistocene Los Gemelos scoria cones were constructed along the Calchaqui fault, NW of Salta. The basaltic trachyandesitic cones produced a lava flow about 35,000 years ago that traveled to the west and then was deflected south. Monogenetic cones at El Saladillo to the NW of Los Gemelos produced a lava flow that traveled to the SE and south.

Antofalla
Volcán Antofalla is a 6409-m-high Argentinian stratovolcano west of the Salar de Antofalla. The andesitic-to-rhyolitic main edifice is surrounded by a circular ring of smaller satellitic stratovolcanoes. Sapper (1917) reported "smoke" clouds from Volcán Antofalla in 1901 and 1911, but detailed study showed that its youngest rocks were erupted during the early Pleistocene (Richards et al., 2006). Younger small-volume monogenetic volcanism took place on the SW and western flanks later in the Pleistocene.

Cerro Galan
Caldera-forming eruption took place about 2.6 million years ago, latest ring fracture eruptions may have taken place in last few tens of thousands of years (Francis 1982).

Cerro Colorado
Cerro Colorado is a stratovolcano of possible Pleistocene age (de Silva, 2007 pers. comm.).

Incapillo
The Plio-Pleistocene Icapillo caldera and lava-dome complex is the southernmost ignimbritic caldera of the Central Andes. The 5 x 6 km wide caldera formed during a rhyodacitic eruption about 510,000 years ago. About 40 rhyodacitic lava domes surround the caldera.

Inacalari
The andesitic stratovolcano Cerro Inacalari is located about 25 km SE of Cerro del Azufre along the Chile-Bolivia border. Satellite imagery shows a small lake in the 400-m-diameter summit crater. It's age was estimated by Gonzales-Ferron (1995) as Pliocene-Pleistocene.

San Felix
Pacific Ocean (Chilean Islands)
San Félix Island, 800 km W of the Chilean coast, consists largely of a low, cliff-bounded lava platform separating two tuff cones. The Islota Gonzáles cone to the SW is separated from the main island by a shallow submerged platform. Cerro Amarillo at the western end forms the high point of the island and is the source of fresh-looking hawaiite lava flows that reached the sea and formed the low lava platform at the SW tip of the island. A ship captain reported a dull red glow at the summit in 1923. Willis and Washington (1924) considered the youthful lava flows to predate discovery of the island in the 16th century, but not be more than a few centuries old. However, Ar-Ar dating by Haase et al. (2000) determined that the adjacent plateau age was 421 +/- 18 ka, and considered the advanced erosion of the island as indicative of several hundred thousands of years of inactivity.

Robinson Crusoe
Pacific Ocean (Chilean Islands)
The main part of Robinson Crusoe (Mas a Tierra) Island, in the central part of the Juan Fernandez Island group, is composed of four overlapping shield volcanoes with calderas breached to the NE. The SW part of the basaltic island consists of smaller altered cones. Potassium-Argon dates for the island range from 5.8 to 3.8 million years ago (Steussy et al., 1984) and the island is more dissected than Alexander Selkirk (Mas a Fuera) Island to the west. An eruption at El Yunque was reported in 1743, but is considered uncertain (Catalog of Active Volcanoes of the World). Reports exist of a submarine eruption about 1.5 km north of the island in 1835 that produced an explosion and flames that lit up the island, primarily from the Governor, but the story varied over the years and no evidence was ever located (see CAVW for summary).

Seamount JF6
Pacific Ocean (Chilean Islands)
A submarine eruption reported in 1839 from a seamount (identified as JF6 by Yanez et al., 2009) at the eastern end of the Juan Fernandez island chain is considered highly suspect (Catalog of Active Volcanoes of the World). Although an ephemeral island was reportedly formed, the seamount has a depth of more than 600 m and lies at the eastern end of an island chain that is progressively younger to the west.

Alexander Selkirk
The dome-shaped island of Alexander Selkirk (Masafuera) is the emergent summit of a Pleistocene shield volcano. A Potassium-Argon date of 1.01 million years ago (Steissy et al., 1984) is the youngest obtained for the Juan Fernandez islands (Stuessy et al., 1984).

Sala y Gomez
Shield?
A small volcanic islet, 400 x 700 m wide, forms the summit of a large seamount. No volcanic vents have been identified, but rocks from the islet are Potassium-Argon dated at 1.94-1.31 million years ago (Clark and Dymond, 1977). Both Easter Island and Scala y Gomez are east of the East Pacific Rise.

Cochiquito Volcanic Group
Central Chile and Argentina
A small group of volcanoes lies N of the town of Buta Ranquil, near where the Río Grande and Río Barrancas join to form the Río Colorado. Volcán Cochiquito is an alkaline basaltic stratovolcano with eight satellitic cones. Volcán Sillanegra (or Malal) is pyroclastic cone complex with two craters and basaltic aa lava flows located east of the Río Grande. Its age was estimated to be Holocene (González-Ferrán, 1995). Volcán Ranquil del Sur is a small stratovolcano south of the Río Barranca with an estimated Pleistocene-Holocene age that contains a 600-m-wide crater and produced andesitic pyroclastic material and lava flows. However, Folguera et al. (2006) describe Chochiquito as being erupted along a normally reactivated reverse fault in the Chos Malal belt, part of a group of basaltic domes and lava flows ranging from 3.2 to 1.5 Ma (citing dates in Linares and Gonzalez, 1987). Other researchers (e.g. Ramos and Folguera, 2011) map the area as older Pleistocene volcanics not part of the larger volcanic fields nearby.

Tupungato
Central Chile and Argentina
The northernmost of the central Chile volcanoes, conical Tupungato is a Pleistocene stratovolcano capped by a about 0.8 million years ago lava dome complex (Moreno and Naranjo 1991).

Nevado de los Piuquenes
Central Chile and Argentina
The Pleistocene volcano Nevado de los Piuquenes is the southernmost volcano of the Tunpungato-Tupungatito volcano group. A 5.5-km-wide amphitheater is open to the east (Moreno and Naranjo 1991).

Northern Mendoza Volcanic Field
The northern part of the Pleistocene Mendoza volcanic field contains more than 80 volcanic centers, mostly basaltic cinder cones, but also the Diamante stratovolcano, a small shield volcano, and tuff rings and tuff cones. The small Infiernillo volcanic field of late-Pleistocene to Holocene age at the SW part of the larger volcanic field is listed separately in this compilation.

Llancanelo Volcanic Field
The Plio-Pleistocene Llancanelo volcanic field lies west of the saline lake of the same name in the Mendoza province of Argentina. The field includes scoria cones, tuff cones, and tuff rings. Often described as covering an area of 10,700 km2, that zone includes the Cerro Nevado and Northern Mendoza volcanic fields.

Sordo Lucas
Sordo Lucas (Alto del Padre) is a highly eroded stratovolcano of Pleistocene age (Moreno and Naranjo, 1991).

Cerro Nevado
The Cerro Nevado Volcanic Field is located north of Payun Matru and west of Llancanelo volcanic field. The exact bounds vary depending on the researcher, with the area between the Cerro Nevado stratovolcano and Payun Matru being considered part of Payun Matru, Cerro Nevado, or the Llancanelo volcanic fields, or simply generically within the Payenia Volcanic Province. K-Ar ages reported by Ramos and Folguera (2011) are around 1.32 Ma.

Puelche Volcanic Field
The Pleistocene Puelche volcanic field is the largest cluster of Quaternary rhyolitic lava flows known to date in the Southern Volcanic Zone of the Andes.

Auca Mahuida Volcanic Field
Auca Mahuida is a large basaltic shield volcano described by Folguera and Ramos (2011) as having a well-preserved central crater and an andesite plug. Most of the lavas, recently date using Ar-Ar, are in the 0.8-1.7 Ma range.

Sierra Nevada
Sierra Nevada is a late-Pleistocene glaciated stratovolcano with a 7-km-long E-W zone of fissure vents that lies about 15 km NE of Llaima volcano. The age of Sierra Nevada has been considered to be late-Pleistocene (Moreno and Naranjo, 1991) or late-Pleistocene to Holocene (González-Ferrán, 1995). Naranjo (pers. comm., 2004) noted that no eruptions have occurred during the Holocene. The volcano has erupted dominantly andesitic to basaltic lava flows and pyroclastic material and has produced pyroclastic flows and lahars.

Pino Hachado
The Pino Hachado caldera in the Nequén Andes of Argentina was constructed along one of the branches of the major regional Liquine-Ofqui fault system. The 12-km-wide caldera is 150 m deep. Following the eruption of dacitic and rhyolitic ignimbrites, post-caldera trachyandesitic lava flows were erupted. Radiometric dates of about 1.6 and 1.2 million years were obtained on post-caldera rocks.

Cerro Trautrén
Cerro Trautrén in Chile lies at the NW end of an area of Pleistocene volcanism along the Chile/Argentina border. The high point of the complex, Cerro Norte Divortium, lies along the border SE of Cerro Trautrén, which has K-Ar dates of about 0.8 and 0.5 million years (Lara et al., 2001).

Nevados de Caburgua
The Nevados de Caburgua group east of Lago Caburgua, has K-Ar dates of 2.4 and 0.8 million years (Lara et al., 2001). The location given by Lara et al. lies east of the location shown on the 1:50,000 topo map.

Cerro Maichín
Lava flows at Cerro Maichín were K-Ar dated at about 0.9 +/- 0.7 million years (Lara et al., 2001).

Quinchilca
The Quinchilca complex south of Villarica volcano is a Pleistocene stratovolcano with a caldera and post-caldera lava domes. A K-Ar date of 0.8 +/- 0.6 million years was obtained by Lara et al. (2001).

Cuernos del Diablo
Southern Chile and Argentina
Cuernos del Diablo is a partially glacially eroded basaltic stratovolcano. Numerous satellitic pyroclastic cones and associated basaltic lava flows were formed during the Holocene, principally on the SW flank and from the summit to the NW base of the volcano. Fumaroles were observed on a flank cone in 1931. Although no historical eruptions are known, some of these cones may have formed during historical time (González-Ferrán, 1995). However, Lara et al. (2001) mapped this volcano as Plio-Pleistocene, and cited a K-Ar age date of 0.7 +/- 0.4 Ma from SERNAGEOMIN-BRGM (1995).

Rio Murta
Southern Chile and Argentina
Basaltic lava flows were emplaced on valley floors along the Río Murta, about 30 km SE of Hudson volcano. The river follows a glacially carved valley cut into granitic rocks of the North Patagonian Batholith. The columnar-jointed lava flows include pillow lavas, lava tubes, and subglacial and sublacustral deposits. They have been considered to be of Holocene age due to lack of erosion and only locally subglacial emplacement. Guivel et al. (2005), however, found that two of three Potassium-Argon dates suggested an age of 850,000-900,00 years, but that a third sample too young to date precisely could be consistent with a Holocene age.

Morne la Vigie
West Indies
Morne la Vigie, a well-preserved nepheline basaltic scoria cone in the Saut d'Eau area north of Port-au-Prince, was dated at about 1.5 million years and represents the youngest volcanism in Haiti (Wadge and Wooden, 1982; Haiti Bureau of Mines and Energy brochure).

Thomazeau
West Indies
Nepheline basaltic pyroclastic cones near the village of Thomazeau, ENE of Port-au-Prince, represent, along with Morne la Vigie to west, the youngest volcanism in Haiti, dated at about 1.5 million years (Wadge and Wooden, 1982; Haiti Bureau of Mines and Energy brochure). Three volcanic episodes happened successively at Thomazeau, and morphologically, the youngest cone is well preserved, with an easily distinguished lava flow.

San Juan
West Indies
Basaltic lava flows of late-Pliocene to late-Pleistocene age up to 10 km long were erupted from scattered cinder cones in the San Juan valley of the western Dominican Republic (Wadge and Wooden, 1982).

Dos Hermanos
The Cerro los Frailes vent, south of the San Juan Los Pozos fault, is adjacent to Dos Hermanos volcanic field, which consists of lava domes and flows of trachy-andesitic composition and is of late-Pliocene to late-Pleistocene age (Wadge and Wooden, 1982).

Valle Nuevo
The Valle Nuevo volcanic field, north of the San Juan Los Pozos fault, consists of late-Pliocene to late-Pleistocene age contains rocks of rhyolitic-to-basaltic composition (Wadge and Wooden, 1982).

South East Range
The South East Range in central St. Kitts is a young volcano with a partly preserved summit crater less than one million years old (Robertson, 2005). The Ottley's Level and Monkey Hill lava domes lie on the flanks of the volcano.

Northern Centres
The Northern Centres volcanic complex consisting of five adjacent volcanic centers forming the NW end of St. Eustatius Island is less than 1 million years old (Smith and Roobol, 2005).

Silver Hills
The Silver Hills volcanic complex at the northern end of Montserrat was active about 2.58-1.16 million years ago (Hincks et al., 2005).

Centre Hills
The andesitic Centre Hills lava-dome complex was active about 0.95-0.55 million years ago (Hincks et al., 2005).

Septentrional Chain
The Septentrional Chain (Northern Chain) of volcanoes at the NW end of Basse Terre consists of andesitic-to-dacitic lava domes and flows that were active from about 3.5 to 1.2 million years ago (Komorowski et al., 2005).

Axial Chain
The Axial Chain in central Basse Terre is a 15-km-long chain of stratovolcanoes that were active about 1.25 to 0.45 million years ago (Komorowski et al., 2005). The youngest eruptions took place at the southern end of the chain, at Sans Toucher volcano. The Bouillante geothermal field was developed along the coast in submarine volcaniclastic rocks.

Bouillante Chain
The Bouillante Chain along the west-central coast of Basse Terre consists of a N-S-trending chain of phreatomagmatic craters and offshore submarine cones that were active about 0.8-0.25 million years ago (Komorowski et al., 2005). The Bouillante geothermal field and numerous submarine hot springs attest to its recent activity.

Monts Caraïbes
The Monts Caraïbes volcanic complex at the southern tip of Basse Terre was active about 0.5 million years ago (Komorowski et al., 2005).

Terre de Bas
Terre de Bas Island, located in the Les Santes Islands off the southern coast of Basse Terre, were active about 1.9-0.6 million years ago (Komorowski et al., 2005).

Foundland
Foundland volcano at the SE tip of Dominica is Pliocene-to-Pleistocene in age. An andesitic lava flow was K-Ar dated at 1.12 million years (Lindsay et al., 2005a).

Pitons de Carbets
The Pitons de Carbets volcanic complex SE of Montagne Pelée, was active during the Pliocene and Pleistocene. The early edifice was cut by a major flank-collapse leaving a breached caldera open to the west, inside which a group of lava domes known as the Pitons were constructed.

A series of small volcanoes was constructed at the SW tip of Martinique about 2-1 million years ago (Komorowski et al., 2005). This group includes the Rocher du Diamant, a lava-dome remnant forming a small island off the south coast of the peninsula.

Morne Garu
Morne Garu stratovolcano, south of Soufrière St. Vincent volcano was active during the Pleistocene. A young Ar-Ar date of 0.011 +/- 0.014 suggests that activity may have overlapped with that of Soufrière St. Vincent volcano (Robertson, 2005b).

Grand Bonhomme
The Grand Bonhomme volcanic centre, along with adjacent South-East volcanics, form much of the southern half of St. Vincent Island. K-Ar dates range from 2.5-1.2 million years (Robertson, 2005b). Pyroclastic cones are found along the southern tip of the island as part of the South-East volcanics and on the western flank of the Grand Bonhomme volcanic centre.

Fagradalsfjall
Iceland (southwestern)
Tuya
Fadradalsfjall is a Pleistocene table mountain in the Reykjanes Peninsula NE of Grindavik.

Grensdalur
Iceland (southwestern)
The small Grensdalur volcanic system (also known as the Hveragerdi system) lies at the eastern end of the Reykjanes Peninsula, SE of the Hengill volcanic system and south of the Hrómundartindur volcanic system. Grensdalur is the oldest of the three volcanic systems in the Hengill area and was last active during the Pleistocene. The Hveragerdi geothermal area contains high- and low-temperature geothermal features that include fumaroles, hot springs and pools, mud pots, and geysers, and provide heat to the town of Hveragerdi.

Lyngdalsheidi
Iceland (southwestern)
Interglacial shield volcano (Thorarinsson 1960).

Geysir
The Geysir volcanic system in the Haukadalur valley of SW Iceland consists of an eroded basaltic central volcano and rhyolitic lava domes of Pleistocene age. Geysers around the world are named for the Geysir geothermal field, which lies SE of the rhyolitic Laugarfjall lava dome and is one of the most frequently visited geological sites in Iceland. No eruptions are known from the Geysir volcanic system during the Holocene.

Hlodufell
Tuya
Hlödufell is a Pleistocene table mountain located ENE of Skjaldbreidur shield volcano.

Thorisjokull
Subglacial
Thorisjökull is a large glacier-covered shield volcano SW of Langjökull volcano.

Ok
The large Ok shield volcano is topped by a small glacial icecap and lies west of the SW tip of Langjökull and NW of Thorisjökull volcano.

Eríksjokull
Tuya
Eríksjökull is a large Pleistocene table mountain located north of Prestahnukur volcano and SW of Langjökull volcano.

Hrutfell
Hrútfell is a Pleistocene ice-capped table mountain east of Langjökull.

Blafell
Bláfell is a Pleistocene table mountain located SW of Kerlingarfjöll volcano.

Hreppar
Two elongated NE-SW-trending Pleistocene hyaloclastite ridges extend from Kerlingarfjöll volcano in the Hreppar area.

Strutur
Iceland (southern)
Strútur is a Pleistocene table mountain located north of Myrdalsjökull.

Tungnaarfjoll
Iceland (northeastern)
An elongated, NW-SE-trending hyaolocasltic ridge of Pleistocene age lies in the Tungnaárfjöll area between the Veidivötn and Laki fissure systems.

Kistufell
Iceland (northeastern)
Kistufell is a Pleistocene table mountain lying NNE of Bardabunga at the margin of Dyngjujökull.

Valdalda
Iceland (northeastern)
Interglacial (Krafft 1974).

Herdubreid
The renowned flat-topped Icelandic table mountain Herdubreid, located NE of Askja volcano, was active until the late Pleistocene.

Sellandafjall
Sellandafjall is a Pleistocene table mountain that lies south of Lake Myvatn, WSW of Fremrinamar volcano.

Blafjall
Bláfjall is a Pleistocene table mountain SE of Lake Myvatn and west of Fremrinamar volcano.

Burfell
Burfell is a Pleistocene table mountain north of Fremrinamar volcano.

Fjallgardar Ridge
The elongated Fjallfadar Ridge is a Pleistocene hyaloclastite ridge that lies on the Pleistocene ice divide east of Fremrinamar volcano.

Gaesafjoll
The Gaesafjöll table mountain of Pleistocene age lies between Krafla and Theistareykhabunga volcanoes.

Lambafjoll
The Lambafjöll fissure vents of Pleistocene age lie west of Theistareykjarbunga volcano.

Snaefell
Iceland (southeastern)
The Snæfell volcanic system, NE of Vatnajökull, has not erupted in the Holocene (Catalogue of Iceland Volcanoes, 2015). This stratovolcano is comprised of rhyolites and evolved basalts built in the last 400,000 years. Volcanic fissures trending NE-SW occur out to 10-18 km from the volcano. It lies on a volcanic belt outside the main volcanic zones. The Snæfell central volcano is Iceland?s highest volcanic peak outside of the large ice caps; it has a small glacier on its summit.

Sigurd
Arctic Ocean
Explosion crater
Semevskii (1965) considered a Holocene age to be a reasonable probability for all the young volcanoes on Spitsbetgen, but more detailed glacial and volcanic stratigraphy indicates that Sigurdfjell is an eroded diatreme of similar age to Sverrefjell,which is considered to be between 100,000 and 250,000 years old (Skjelkvale et al. 1989).

Halvdan
Arctic Ocean
A Holocene age was considered reasonably probable for all the young volcanoes of Spitsbergen by Semevskii (1965), but more detailed glacial and volcanic stratigraphy indicates that Halvdan is an eroded diatreme probably older than Sverrefjell, which is thought to be between 100,000 and 250,000 year old (Skjelkvale et al. 1989).

Sverrefjell
Arctic Ocean
Early investigators considered Sverre to be of postglacial age based on its location in a glacially carved valley. Semevskii (1965) assigned an age between 6500 and 4000 years before present (BP) marine terraces. A more detailed study of glacial and volcanic stratigraphy suggests an age between 100,000 and 250,000 BP (Skjelkvale et al. 1989).

Sao Vicente
Cape Verde Islands
The 15 x 25 km island of Sao Vicente contains mafic lavas covering prominent peninsulas on the eastern and NE sides (Mitchell-Thome, 1976). The largest indentation on this island with an irregular shoreline is formed by a caldera on the NW coast that is breached by the sea and forms the setting for the port of Mindelo, the island's largest village. No Holocene material has been dated, and as of 2015 scientists in Cape Verde consider it's last activity to have been in the Pleistocene.

Santo Antao
Cape Verde Islands
The 20 x 40 km dominantly volcanic island of Santo Antao is the NW-most of the Cape Verde Islands. Volcanic activity dates back to the Pliocene and continued into the late Pleistocene. A large 7-km-wide E-facing depression, Cha de Morte, was thought at one point to be a caldera, but was later interpreted as an erosional feature. Much of the island is covered by phonolitic pumice deposits of the Cao Grande Pumice, erupted about 200,000 years ago. The youngest eruptive products are lava flows that originated from vents at Cha de Lagoa in the central part of the island, just south of the NE-SW axial ridge. The lava flows cover an area of 40 km2 and reached the SE coast just SW of the coastal village of Porto Novo. These flows were initially considered by Mitchell-Thome (1976) to be Holocene in age based on morphological evidence, but later 40Ar/39Ar dating by Plesner et al. (2003) for these lava flows produced an age of 90,000 +/- 30,000 years.

Sao Nicolau
Cape Verde Islands
Sao Nicolau, located the eastern end of an E-W-trending chain of islands in the NW Cape Verde islands, was constructed in four stages dating back to the Pliocene. The last two stages took place during the Pleistocene, and the youngest stage produced scoria cones and lava flows about 50,000 years ago.

Trindade
Atlantic Ocean (central)
The small island of Trindade lies more than halfway between Brazil and the Mid-Atlantic Ridge at the eastern end of the Vitória-Trindade Ridge, an E-W-trending chain of submarine volcanoes and guyots extending about 1,100 km from the continental shelf off the Brazilian coast. It is a dissected volcanic island with numerous phonolitic lava domes and steep-sided volcanic plugs. The youngest volcanism, at Vulcao de Paredao on the SE tip of the island, constructed a pyroclastic cone with lava flows (Almeida, 1961). Remnants of the crater of the cinder cone are still preserved. Lava flows traveled from the cone to the N, where they form an irregular shoreline and offshore islands. Smaller centers of the latest volcanic stage are found in the Morro Vermelho area in the south-central part of the island.

Martin Vaz
Atlantic Ocean (central)
The Martin Vaz archipelago lies 48 km east of Trindade Island, about 1750 km west of the Mid-Atantic Ridge. A larger islet, Martin Vaz, is adjacent to three smaller ones. K-Ar ages of about 1.5 Ma and <0.73 Ma were obtained.

Gough Island
Atlantic Ocean (southern)
Gough Island, also known as Diego Alvarez, lies about 340 km SE of the Tristan da Cunha island group. The shield volcano was active from about 2.5 to 0.13 million years ago.

Inaccessible Island
Atlantic Ocean (southern)
Inaccessible Island, located about 40 km SW of Tristan da Cunha, was Potassium-Argon age dated at 6 +/- 1.5 million years ago (Baker et al., 1964), but more recent dates of about 1 million have been obtained (Cliff et al., 1991). The island is the remnant of a stratovolcano centered about 2 km SW.

Antarctica and South Sandwich Islands
A large number of isolated basaltic scoria cones are located throughout Antarctica's northern Victoria Land near the western coast of the Ross Sea, not clearly associated with the larger stratovolcanoes. One lava flow on the southern side of Cosmonaut Glacier, SW of Mount Overlord, spilled onto the glacier and diverted it, but has not yet been removed by erosion or covered by ice. Nathan and Schulte (1968) inferred a possible age for the lava flow of less than a thousand years, but not greater than 50 ka. Potassium-Argon dates from Overlord (see separate volcano entry) indicate an age of about 7 million years ago (Kyle 1977, pers. comm., LeMasurier and Thomson 1990). There is no clear evidence of Holocene activity from any of these poorly-studied basaltic rocks, called the "Local Suite" by Nathan and Shulte (1968).

Gaussberg
Antarctica and South Sandwich Islands
Gaussgberg is an ice-free conical mountain composed primarily of subglacial eruptive products. No vent has been located and its present morphology is thought to result from glacial and subaerial erosion of a once-larger mountain that was formed about 55,000 years ago (LeMasurier and Thomson 1990).

Adare Peninsula
Antarctica and South Sandwich Islands
The Adare Peninsula is a complex of overlapping shield volcanoes forming the northernmost volcanic pile of the Hallet Volcanic Province. Hamilton (1972) considered uneroded cinder cones at Cape McCormick to be of Holocene age, but similar-looking Antarctic cones have proved to be as old as Tertiary. Most Potassium-Argon dates for the Adare Peninsula range from 6-13 million years ago (Ma), but one possibly anomalous date of 1.14 Ma was obtained, and a sample from Cape Roget was dated at 2.27 Ma (LeMasurier and Thomson, 1990).

Mount Rittmann
Mount Rittmann, a roughly 8 x 5 km caldera under the Aviator Glacier in the Melbourne Volcanic Province, has been dated at between about 4 and 0.07 million years ago (Martin et al., 2010). Active fumaroles, heated ground, and ice and snow hummocks occur near the caldera rim.

Franklin Island
Franklin Island is a 2 x 7.6 km remnant of a shield volcano whose vent was located to the east. IAVCEI (1973) assigns a Quaternary age. The only radiometric date available is a Potassium-Argon date of 4.8 +/- 2.0 Ma (LeMasurier and Thomson 1990). Bathymetric mapping in 2004 identified the Franklin Volcanic Field, a regional high with clusters of submarine cones extending 80 km long and up to 40 km wide (Smith, 2004).

Beaufort Island
Beaufort Island is an eroded remnant of a Quaternary volcano (Calkin and Nichol 1972). LeMasurier and Thomson (1990) indicate its age is unknown.

Terror
Mount Terror is a large basaltic shield volcano forming the eastern portion of Ross Island with numerous pyroclastic cones and lava domes. The youngest dated rocks are 0.82 million years ago (Ma) from the lower slopes of Terror and 0.8 Ma from the summit of Terra Nova, a large basaltic cone on the W flank (LeMasurier and Thomson, 1990).

Taylor Valley
Taylor Valley contains numerous basaltic cinder cones, the youngest of which is Potassium-Argon dated 1.57 million years ago. Similar Pliocene volcanism took place in the Wright Valley to the north (LeMasurier and Thomson 1990).

Bursey
Latitude: 76°S
Two coalescing shield volcanoes with 4-5 km diameter summit calderas, Hutt Peak on the east and Koerner Bluff on the west, form Mount Bursey. Potassium-Argon dates indicate both volcanoes were constructed during the Miocene; the youngest dated rock is 0.49 million years old, from a parasitic cone vent on the Hutt Peak caldera rim (LeMasurier and Thomson, 1990).

Obiglio
Mt. Obiglio is a strombolian-phreatomagmatic cone on Grant Island with a Potassium-Argon date of 0.51 million years ago (LeMasurier and Thomson, 1990).

Shepard Island
Tuff cone(s)
Shepard Island consists of a group of tuff cones and a possible lava dome. The youngest dated rock at Worley Point has a Potassium-Argon date of 0.42 million years ago (LeMasurier and Thomson 1990).

Crary Group
The Crary Mountains consist of two large shield volcanoes, Mount Frakes and Mount Steere and the smaller Mount Rees and Boyd Ridge volcanoes. Mount Steere is dissected, but the younger Mount Frakes is relatively undissected has had flank vent activity as late as 1.7 million Potassium-Argon years ago (LeMasurier and Thomson, 1990).

Murphy
Mount Murphy is a glacially dissected basaltic-trachytic shield volcano that formed during the Miocene. A Potassium-Argon date on a parasitic cone of 0.9 million years ago indicates that flank activity resumed much later during the Pleistocene (LeMasurier 1972, LeMasurier et al. 1990).

Beethoven Peninsula
The Beethoven Peninsula contains nine nunataks consisting of basaltic lava flows and associated hyaloclastites. No primary volcanic edifice is preserved and it is not clear whether the exposures represent individual volcanic vents or a volcanic field. The youngest dated rocks are less than one million years old (LeMasurier and Thomson 1990).

Brabant Island
Isolated exposures of the Bahia Bouquet Formation occur on Brabant Island; a Potassium-Argon date of less than 1 million years ago was obtained from a rock at the northern end of the island. The region has been poorly studied (LeMasurier and Thomson 1990).

Hut Point Peninsula
Hut Point Peninsula consists of a 20-km-long line of basaltic scoria cones south of Erebus. Potassium-Argon dates range from 0.44 to 1.34 million years ago (LeMasurier and Thomson, 1990). Martin et al. (2010) listed a 0.5 Ma date.

White Island
White Island is a mostly ice-covered volcanic complex at the northern end of the island consisting of two shield volcanoes and overlying pyroclastic cones. The youngest Potassium-Argon date obtained was 0.17 million years ago and there is no evidence of Holocene activity.

Black Island
A series of basaltic pyroclastic cones and trachytic lava domes form Black Island, in the Ross Sea west of White Island. Potassium-Argon dates of 3.4 Ma were obtained (LeMasurier and Thomson 1990). Martin et al. (2010) reported dates of 3.8-1.69 million years.

Transantarctic Mountain Foothills
Volcanic rocks in the Transantarctic Mountain Foothills have been radiometrically dated at between 14 and 0.9 million years (Martin et al., 2010).

Mason Spurr
An older trachytic volcanic complex at Mason Spurr is overlain by a younger volcanic sequence consisting of a trachytic dome and tuff rings and numerous basanite and tephrite cinder cones. Several lava flows drape over the Mason Spurr bluffs, and may be less than 100,000 years old (LeMasurier and Thomson, 1990).

Livingston-Greenwich Islands
Several small eroded tuff cones remnants and volcanic plugs are located on northern Livingston and Greenwich Island. Dated samples from two location are younger than 0.5 million years ago (LeMasurier and Thomson 1990).

Tabarin Peninsula
Shield?
Extensive plateau basalts on the southern Tabarin Peninsula may have erupted from fissures, small centers, or a large shield volcano. Basalts and tuff breccias are also found on Jonassen, Andersson, Rosamel and Dundee Islands. The only radiometric ages are 1.1 and 0.9 million years ago from rocks on the Tabarin Peninsula (LeMasurier and Thomson 1990).

Argo Point
Argo Point is a small scoria cone on the Jason Peninsula for which Potassium-Argon dates of 1.4 and 0.9 million years ago have been obtained (LeMasurier and Thomson, 1990).

Discovery
Mount Discovery is central volcano that formed about 5.3 million Potassium-Argon years ago. The youngest parastic cones have been dated at about 1.87 million years ago (LeMasurier and Thomson, 1990).