The inception and progression of melting in a monogenetic eruption: Motukorea Volcano, the Auckland Volcanic Field, New Zealand

McGee, Lucy; Millet, Marc-Alban; Smith, I. E.; Németh, Károly; Lindsay, Jan M.

doi:10.1016/j.lithos.2012.09.012

Cited by 71 publications

(46 citation statements)

References 61 publications

Supporting

Mentioning

Contrasting

Order By: Relevance

“…Brenna et al 2010), different degrees of partial melting at similar depths (e.g. McGee et al 2012), different degrees of fractionation of magma during rise (e.g. Smith et al 2008;Murcia et al, JVGR, under review), fractional crystallisation± assimilation related to stagnation (e.g.…”

Section: Whole-rock Geochemistrymentioning

confidence: 99%

The Al-Du’aythah volcanic cones, Al-Madinah City: implications for volcanic hazards in northern Harrat Rahat, Kingdom of Saudi Arabia

et al. 2015

View full text Add to dashboard Cite

The basaltic Al-Du'aythah volcanic cones lie in the northern part of the extensive lava field of Harrat Rahat, and only 13 km from the centre of Al-Madinah City, in the Kingdom of Saudi Arabia. Historical records indicate they may have erupted in AD 641. The four cones are formed by deposits that record a transition from phreatomagmatic to magmatic explosions followed by minor lava effusion. Three cones display elongated tuff rings at the base, and two produced late-stage lava flows. The cones themselves are symmetrical and constructed mostly by the accumulation of ballistically ejected pyroclasts. Spherical bombs and lapilli (cannonball bombs/lapilli), occasionally with country-rock fragments inside (both cored and loaded bombs/lapilli) are common within the tuff ring deposits. LiDAR data show a total volume of 1,664×10 −6 km 3 for the four cones (418×10 −6 km 3 DRE). Whole-rock chemical analyses indicate alkali-basalt compositions (SiO 2 44.7-45.9 wt%), with little compositional variation and no relationship between chemistry and eruptive styles. Small differences in composition may reflect variations in fractional crystallisation of clinopyroxene and olivine. A magnetotelluric 2D cross-section shows that the cones are located adjacent to a buried sediment-filled alluvial channel along a NNW-SSE fault dipping to the east. The AlDu'aythah eruption was related to the ascent of magma through this structure, with the first phase of the eruption triggered by the interaction of the magma with water from the northern Harrat Rahat aquifer that exists in the AlMadinah basin. This initial water source was rapidly exhausted, while the eruption progressed roughly from north to south and from west to east, the latter motion probably along the fault-controlled feeding dyke. Our work draws attention to the existence of recent explosive phreatomagmatic eruptions in the Al-Madinah basin, which, despite the hyperarid climate of the area, must be considered a potential future eruption hazard.

show abstract

Section: Whole-rock Geochemistrymentioning

confidence: 99%

The Al-Du’aythah volcanic cones, Al-Madinah City: implications for volcanic hazards in northern Harrat Rahat, Kingdom of Saudi Arabia

et al. 2015

View full text Add to dashboard Cite

show abstract

“…52 This study shows that high-resolution mineral-scale analyses carried out through monogenetic sequences 53 provide a unique, more detailed insight into the evolution of these "simple" magmatic systems as crystal growth 54 stratigraphy and compositions yield direct evidence for various petrogenetic processes which are usually 55 obscured in the whole-rock geochemistry. ing ascent (e.g., Strong and Wolff, 2003; Brenna et al, 2010 Brenna et al, , 2011 Erlund 77 et al, 2010;Mcgee et al, 2012; Sohn et al, 2012; Boyce et al, 2015). …”

mentioning

confidence: 99%

A complex magmatic system beneath the Kissomlyó monogenetic volcano (western Pannonian Basin): evidence from mineral textures, zoning and chemistry

Jankovics

Harangi

Németh

et al. 2015

Journal of Volcanology and Geothermal Research

Self Cite

View full text Add to dashboard Cite

22Kissomlyó is a small-volume Pliocene alkaline basaltic eruptive centre located in the monogenetic Little 23 Hungarian Plain Volcanic Field (western Pannonian Basin). It consists of a sequence of pyroclastic and 24 effusive eruptive units: early tuff ring (unit 1), pillow and columnar jointed lava (unit 2), spatter cone 25 (unit 3). The tuff ring sequence is overlain by a unit of lacustrine sediments which suggests a significant 26 time gap in the volcanic activity between the tuff ring formation and the emplacement of the lava flow.27 High-resolution investigation of mineral textures, zoning and chemistry as well as whole-rock geochemical 28 analyses were performed on stratigraphically controlled samples in order to characterise the magmas 29 represented by the distinct eruptive units and to reveal the evolution of the deep magmatic system. 30 Based on the bulk rock geochemistry, compositionally similar magmas erupted to the surface during the entire 31 volcanic activity. However, olivine crystals show diverse textures, zoning patterns and compositions reflecting 32 various deep-seated magmatic processes. Five different olivine types occur in the samples. Type 1 olivines 33 represent the phenocryst sensu stricto phases, i.e., crystallised in situ from the host magma. The other olivine 34 types show evidence for textural and compositional disequilibrium reflecting single crystals consisting of distinct 35 portions having different origins. Type 2a and type 2b olivines have antecrystic cores which are derived from two 36 distinct primitive magmas based on the different compositions of their spinel inclusions. Type 4 olivines show 37 reverse zoning whose low-Fo cores represent antecrysts from more evolved magmas. The cores of type 3 and 38 type 5 olivines are xenocrysts originated from the subcontinental lithospheric mantle. These xenocrysts are 39 surrounded by high-Fo or low-Fo growth zones suggesting that olivine xenocryst incorporation occurred at 40 different levels and stages of magma evolution. 41 Olivine-hosted spinel inclusions show three distinct compositional groups. Group 1 spinels are very Al-rich 42 (0-0.22 Cr#) and coexist with the antecrystic cores of type 2a olivines, group 2 spinels have 44.5-62.3 Cr#s 43 and occur in the phenocryst s.s. (type 1) olivines, while group 3 spinels are very rich in 44 and appear in the antecrystic cores of type 2b olivines. Based on the integrated analysis of olivines and their 45 spinel inclusions four magmatic environments were involved into the evolution of the magmatic system. 46 These crystals bear evidence of various petrogenetic processes playing role in the formation of the erupted 47 magma batches: fractional crystallization, olivine (+ spinel) recycling, xenocryst incorporation, magma 48 recharge and interaction of multiple small magma packets in a multi-level magmatic system. 49 Clinopyroxene-melt thermobarometry yields an average pressure of 6.6 ± 0.9 kbar corresponding to a depth of 50 about 25 km, implying that the main level of final clinopyroxene fr...

show abstract

“…These included monogenetic volcanoes sensu stricto and complex monogenetic volcanoes with multiple eruptive episodes, which in some cases are characterized by a complex magmatic feeding system. In the literature there are numerous examples for such eruptive behavior: Crater Hill [32], the long-lived scoria cone and lava flow complex of Rangitoto Auckland volcanic field, New Zealand [86], and Motukorea tuff ring in Auckland volcanic field, New Zealand [87,88]; the Kissomlyó in Hungary (e.g., [89]); the Udo, Songaksan, and Yangpory in South Korea (e.g., [8,54,90]); the Purrumbete Maar in Australia (e.g., [10]); Fekete-hegy [91], Bondoró [31], and Tihany [29] from the BakonyBalaton Highland Volcanic Fields in Western Hungary; some maars in the Eifel volcanic field, Germany [92,93]; the Cerro Negro scoria cone, Nicaragua [94,95]; and El Volcancillo, Mexico [96]. All of these examples were likely constructed over a longer period of time (from Ky to My).…”

Section: Features Of Complex Maar Volcanoesmentioning

confidence: 99%

How Polygenetic are Monogenetic Volcanoes: Case Studies of Some Complex Maar‐Diatreme Volcanoes

Tchamabé¹,

Keresztúri²,

Németh³

et al. 2016

Updates in Volcanology - From Volcano Modelling to Volcano Geology

View full text Add to dashboard Cite

The increasing number of field investigations and various controlled benchtop and largescale experiments have permitted the evaluation of a large number of processes involved in the formation of maar-diatreme volcanoes, the second most common type of smallvolume subaerial volcanoes on Earth. A maar-diatreme volcano is recognized by a volcanic crater that is cut into country rocks and surrounded by a low-height ejecta rim composed of pyroclastic deposits of few meters to up to 200 m thick above the syn-eruptive surface level. The craters vary from 0.1 km to up to 5 km wide and vary in depth from a few dozen meters to up to 300 m deep. Their irregular morphology reflects the simple or complex volcanic and cratering processes involved in their formation. The simplicity or complexity of the crater or the entire maar itself is usually observed in the stratigraphy of the surrounding ejecta rings. The latter are composed of sequences of successive alternating and contrastingly bedded phreatomagmatic-derived dilute pyroclastic density currents (PDC) and fallout depositions, with occasional interbedded Strombolian-derived spatter materials or scoria fall units, exemplifying the changes in the eruptive styles during the formation of the volcano. The entire stratigraphic sequence might be preserved as a single eruptive package (small or very thick) in which there is no stratigraphic gap or significant discordance indicative of a potential break during the eruption. A maar with a single eruptive deposit is quantified as monogenetic maar, meaning that it was formed by a single eruptive vent from which only a small and ephemeral magma erupted over a short period of time. The stratigraphy may also display several packages of deposits separated either by contrasting discordance surfaces or paleosoils, which reflect multiple phases or episodes of eruptions within the same maar. Such maars are characterized as complex polycyclic maars if the length of time between the eruptive events is relatively short (days to years). For greater length of time (thousands to millions of years), the complex maar will be quantified as polygenetic. These common depositional breaks interpreted as signs of temporal interruption of the eruptions for various timescales also indicate deep magma system processes; hence magmas of different types might erupt during the formation of both simple and complex maars. The feeding dikes can interact with groundwater and form closely distributed small craters. The latter can coalesce to form a final crater with various shapes depending on the distance between them. This observation indicates the significant role of the magmatic plumbing system on the formation and growth of complex and polygenetic maar-diatreme volcanoes.

show abstract

The inception and progression of melting in a monogenetic eruption: Motukorea Volcano, the Auckland Volcanic Field, New Zealand

Cited by 71 publications

References 61 publications

The Al-Du’aythah volcanic cones, Al-Madinah City: implications for volcanic hazards in northern Harrat Rahat, Kingdom of Saudi Arabia

The Al-Du’aythah volcanic cones, Al-Madinah City: implications for volcanic hazards in northern Harrat Rahat, Kingdom of Saudi Arabia

A complex magmatic system beneath the Kissomlyó monogenetic volcano (western Pannonian Basin): evidence from mineral textures, zoning and chemistry

How Polygenetic are Monogenetic Volcanoes: Case Studies of Some Complex Maar‐Diatreme Volcanoes

Contact Info

Product

Resources

About