Coarse-grained nonmarine volcaniclastic sediment: Terminology and depositional process

Smith, Gary A.

doi:10.1130/0016-7606(1986)97<1:cnvsta>2.0.co;2

Cited by 457 publications

(310 citation statements)

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“…We suggest that the studied tuff ring deposit was formed by multiple (periodic) flows of a hyperconcentrated water pyroclastic mixture, which moved radially from the crater area (Smith, 1986). The absence of scour and channelling indicates that the flows were depositional and unconfined.…”

Section: Tuff Ring Depositsmentioning

confidence: 86%

“…The muddy layers settled out from temporary lakes that formed with each lahar event. The grain size and bedding characteristic of the deposits shows that both lahars had relatively low concentrations of solid particles and were hyperconcentrated flood flows (Smith, 1986).…”

Section: Laharsmentioning

confidence: 99%

“…Thus, the upper gas-pyrodaslic surge was a transport system, which contributed material to the lower waterpyroclast underflow, which was the depositional system (Fisher, 1990). Deposition from the underflow was similar to deposition from hyperconcentrated flood flow (Smith, 1986).…”

Section: Ejection and Depositionmentioning

confidence: 99%

“…Deposition from the underflow is akin to deposition from hyperconcentrated flood flow (Smith, 1986). The deposits of water-rich surges have an extremely low content of fines, and have none of the wave laminations that are characteristic of many base-surge deposits.…”

Section: O N C L U S I O N Smentioning

confidence: 99%

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Eruptive Process, Effects and Deposits of the 1996 and the Ancient Basaltic Phreatomagmatic Eruptions in Karymskoye Lake, Kamchatka, Russia

Belousov

Belousova

2001

Volcaniclastic Sedimentation in Lacustrine Settings

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On 2-3 January 1996 an explosive eruption discharging = l0 6 kgs -1 of basaltic magma occurred in Karymskoye lake at an initial water depth of ~ 50 m. Characteristics of the deposits together with analyses of a videotape of several explosions have allowed us to model the eruptive events. Initial vent-clearing phreatic explosions ejected blocks of country rocks (up to 3 m diameter) to distances of up to 1.3 km. Then followed 10-20 h of phreatomagmatic Surtseyan activity (100-200 outbursts of water-gas-pyroclastic mixtures to heights of up to 1 km, with initial velocities of 110 m s -1 |. The eruption slugs collapsed back into the lake and produced base surges (runout up to 1.3 km; average velocity 12.5 m s -1 ). The convective eruption plume rose to a height of 3 km and deposited a thin distal fall deposit. The eruption ended with the ejection of scoria-crust bombs (specific basaltic bombs with dense core and scoriaceous crust).Pyroclasts of the eruption are mostly poorly to moderately vesicular juvenile basaltic particles shaped by a combination of magmatic vesiculation and magma-water interaction. Ninety-five percent of the products (0.047 km 3 ) formed an underwater tuff ring composed of parallel layers of moderately to poorly sorted lapilli ash and ash lapilli (Md -3.9 to 0.6 phi; sorting 1.5-3.2 phi), each 10-60 cm thick. They were deposited by water-rich base surges that originated from Surtseyan type eruption bursts. The most widespread hazards of the eruption were tsunamis and lahars. At distances < 1.3 km from the crater, base surges and ballistic clasts were very destructive.Eruptive activity in the lake before 1996 included two eruptions at c. 4800 14 C yr BP. The first left deposits similar to those of the 1996 eruption and thus is interpreted as a Surtseyan eruption that occurred at the same water depth as in 1996. The second of the 4800 l4 C yr BP eruptions deposited extensive cross-laminated base-surge deposits and is interpreted to have occurred in very shallow water.

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Section: Tuff Ring Depositsmentioning

confidence: 86%

Section: Laharsmentioning

confidence: 99%

Section: Ejection and Depositionmentioning

confidence: 99%

Section: O N C L U S I O N Smentioning

confidence: 99%

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Eruptive Process, Effects and Deposits of the 1996 and the Ancient Basaltic Phreatomagmatic Eruptions in Karymskoye Lake, Kamchatka, Russia

Belousov

Belousova

2001

Volcaniclastic Sedimentation in Lacustrine Settings

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“…The massive pebbly sandstone (facies Sma; Mueller and others, 1994) at the base of the sequence may be a hyperconcentrated flood or sheetflow deposit (Flint and others, 1986;Smith, 1986;Horton and Schmitt, 1996). Matrix-supported conglomerates (facies Gms) with subangular to subrounded clasts are typical of debris flow deposits (Schulz, 1984;Mack and Rasmussen, 1984).…”

Section: Conglomerate Facies Association-i (Cfa-i)mentioning

confidence: 99%

Implications of an archean strike-slip basin :

Corcoran¹

1996

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RESUMELa formation de Beaulieu Rapids est une séquence sédimentaire de 0,2 à 1 km d'épaisseur située au centre-sud de la Province structurale de l'Esclave. La formation représente un bassin en décrochement archéen qui s'est développé le long d'une faille majeure de direction NS. Des petits plutons de porphyres quartzo-feldspathiques à hornblende sont localisés le long de la zone de faille. Des datations U-Pb sur zircons donnent un âge approximatif de 2.6 Ga pour ces plutons. La présence de fragments de porphyres dans les conglomérats indique que la formation de Beaulieu Rapids doit conséquemment être plus jeune que cet âge. La marge ouest du basin est caractérisée par une discordance que sépare la ceinture volcanique de Rivière Beaulieu de la succession sédimentaire. Des failles NE tardives sont présentes sur les bordures nord et sud du bassin.Structuralement, la formation est caractérisée par une foliation penetrative NNE et par des plis en échelons dont l'orientation dominante est aussi NNE. Les plis se présentent sous la forme d'une alternance d'anticlinaux et de synclinaux localisés majoritairement dans la partie nord du bassin. Dans ce secteur, la direction de la polarité change rapidement alors que dans la partie sud du bassin les lits sont de direction nord avec une polarité généralement vers l'est. Quelques lits sont renversés mais les lits normaux sont plus communs.Les roches sédimentaires du bassin de Beaulieu Rapids montrent deux cycles positifs qui indiquent un contrôle tectonique sur la sédimentation. Le premier cycle est représenté par l'association de faciès du conglomérat I (CFA-I: Conglomerate faciès association I) et le faciès de siltstone-grès sus-jacent (SSFA: Siltstone-sandstone faciès association). L'association de faciès du conglomérat II (CFA-II: Conglomerate faciès association H) et l'association de faciès de grès riche en quartz (QSFA: Quartz-rich sandstone faciès association) qui se trouve juste au-dessus forment ensemble le second cycle de dépôt. Le CFA-I regroupe un conglomérat à cailloux et galets massif à stratifié et un conglomérat à support de matrice. Le premier est caractérisé par des conglomérats massifs à faiblement stratifiés (faciès Gm) et à lits entrecroisés en forme de fosse (Gt) à support de fragments, des conglomérats massifs à support de matrice (Gms), une unité mineure de grès à stratifications horizontales (faciès Sh) et entrecroisées (faciès St, Sp) et une argilite (FI). Localement, les galets deviennent imbriqués et montrent une composante d'écoulement NE prononcée. Le conglomérat massif à stratifié à cailloux et galets se compose des faciès Gm, Gt, Gp, St, Sh et Sp. Le CFA-I a été déposé par coulées de débris (Gms), courants de traction (Gm-Gt-StSp-Sh) et coulées en feuillets respectivement sur les portions proximale, médiale et distale du cône alluvionnaire. L'association de faciès du siltstone-grès contient une sous-unité dominée par des grès et caractérisée par les faciès Sp, St, Sh et FI qui se sont formés en raison de la migration des dunes et dépôts de levée...

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Geomorphic effects of large debris flows on channel morphology at North Fork Mountain, eastern West Virginia, USA

Cenderelli

Kite

1998

Earth Surf. Process. Landforms

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Extreme rainfall in June 1949 and November 1985 triggered numerous large debris flows on the steep slopes of North Fork Mountain, eastern West Virginia. Detailed mapping at four sites and field observations of several others indicate that the debris flows began in steep hillslope hollows, propagated downslope through the channel system, eroded channel sediment, produced complex distributions of deposits in lower gradient channels, and delivered sediment to floodwaters beyond the debris-flow termini. Based on the distribution of deposits and eroded surfaces, up to four zones were identified with each debris flow: an upper failure zone, a middle transport/erosion zone, a lower deposition zone, and a sediment-laden floodwater zone immediately downstream from the debris-flow terminus. Geomorphic effects of the debris flows in these zones are spatially variable. The initiation of debris flows in the failure zones and passage through the transport/erosion zones are characterized by degradation; 2300 to 17 000 m 3 of sediment was eroded from these zones. The total volume of channel erosion in the transport/erosion zones was 1·3 to 1·5 times greater than the total volume of sediment that initially failed, indicating that the debris flows were effective erosive agents as they travelled through the transport/erosion zones. The overall response in the deposition zones was aggradation. However, up to 43 per cent of the sediment delivered to these zones was eroded by floodwaters from joining tributaries immediately after debris-flow deposition. This sediment was incorporated into floodwaters downstream from the debris-flow termini causing considerable erosion and deposition in these channels.

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Coarse-grained nonmarine volcaniclastic sediment: Terminology and depositional process

Cited by 457 publications

References 0 publications

Eruptive Process, Effects and Deposits of the 1996 and the Ancient Basaltic Phreatomagmatic Eruptions in Karymskoye Lake, Kamchatka, Russia

Eruptive Process, Effects and Deposits of the 1996 and the Ancient Basaltic Phreatomagmatic Eruptions in Karymskoye Lake, Kamchatka, Russia

Implications of an archean strike-slip basin :

Geomorphic effects of large debris flows on channel morphology at North Fork Mountain, eastern West Virginia, USA

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