The effect of recent volcanic events and climatic changes on the vegetation of Mt Egmont (Mt Taranaki), New Zealand

McGlone, Matt S.; Neall, Vincent E.; Clarkson, Bruce D.

doi:10.1080/0028825x.1988.10410105

Cited by 52 publications

(30 citation statements)

References 11 publications

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“…Also, at the same site, a maximum age (NZ3139A) of 3320 ± 60 years B.P. is established from radiocarbon dating of peat c. 1.9 m beneath the lower contact of Manganui tephra (McGlone et al 1988). Assuming a uniform peat accumulation rate between the two radiocarbon dates, Manganui tephra is here estimated to have an age of between 3050-3100 years B.P.…”

Section: Agementioning

confidence: 99%

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Late Quaternary (post 28,000 year B.P.) tephrostratigraphy of northeast and central Taranaki, New Zealand

Alloway

Neall

Vucetich³

1995

Journal of the Royal Society of New Zealand

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109

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Mt. Egmont/Taranaki in western North Island, New Zealand, has been inactive during historic time and thus its pattern of eruptive history must be reconstructed by inference from the stratigraphy and chronology of associated volcanic and pyroclastic deposits. The most complete record of eruptive activity from Egmont Volcano is found on the surrounding ring plain rather than on the volcanic cone, where surficial deposits are readily removed by erosion or deeply buried by the products of more recent eruptions. In this study, a comprehensive post-28 ka record of the volcano's eruptive history is presented, and the relationship of andesitic tephra beds to andic soil material, Egmontsourced volcaniclastic detritus, and two silicic tephra beds from Taupo Volcano are discussed, along with implications for inter-regional correlation.The post-28 ka tephra succession is recorded in sixteen andesitic tephra formations. These formations and their approximate ages are as follows: Manganui tephra (4 beds;

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Section: Agementioning

confidence: 99%

“…2). These beds comprised the informally defined Kaupokonui, Maketawa and Manganui tephras (McGlone et al 1988) which overlie the formally defined Inglewood and Korito Tephras (Neall 1972). These in turn overlie the informally defined E5 (youngest), E4, E3, E2, El and Mahoe (oldest) tephra units (Franks 1984).…”

Section: Study Areamentioning

confidence: 99%

Late Quaternary (post 28,000 year B.P.) tephrostratigraphy of northeast and central Taranaki, New Zealand

Alloway

Neall

Vucetich³

1995

Journal of the Royal Society of New Zealand

Self Cite

109

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“…3c) (e.g. Nicholls 1959;McGlone et al 1988;Newnham & Lowe 1991;Lees & Neall 1993;Wilmshurst & McGlone 1996). The 1850 years BP Taupō eruption, for example, overwhelmed 20 000 km 2 of forest with ignimbrite, and damaged forests up to 170 km east of the vent with windblown ash-fall (Pullar et al 1977;Wilmshurst & McGlone 1996).…”

Section: New Zealand Forest Disturbance Regimes Geological and Geomormentioning

confidence: 99%

New Zealand forest dynamics: a review of past and present vegetation responses to disturbance, and development of conceptual forest models

Wyse¹,

Wilmshurst²,

Burns³

et al. 2018

NZ J Ecol

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New Zealand forests have been and are shaped by a suite of disturbance types that vary in both their spatial extent and frequency of recurrence. Post-disturbance forest dynamics can be complex, non-linear, and involve multiple potential pathways depending on the nature of a perturbation, site conditions, and history. To capture the full range of spatial and temporal dynamics that shape forest ecosystems in a given area, we need to use and synthesise data sources that collectively capture all the relevant space-time scales. Here we integrate palaeoecological data with contemporary ecological evidence to build conceptual models describing post-disturbance dynamics in New Zealand (NZ) forests, encompassing large temporal and spatial scales. We review NZ forest disturbance regimes, focussing primarily on geological and geomorphic disturbances and weather-related disturbances but also considering the role of anthropogenic disturbance in shaping present-day NZ forests. Combining information from 58 studies of post-disturbance forest succession, we derive conceptual models and describe forest communities and forest change for conifer-angiosperm (including kauri forest), and beech forests (pure and mixed). The methods used in these studies included chronosequences, assessments of stand dynamics, longitudinal studies, palaeoecological reconstructions, and comparisons with historical observations; the temporal range of the studies extended from 15 years to millennia (c. 14 000 years BP). Our models capture the generalities of NZ forest dynamics, and can be used to support modelling and help guide decision-making in areas such as ecosystem restoration. However, this generality limits model resolution, meaning the models do not always portray the specific features of individual sites and successional pathways. There is, therefore, scope for more detailed, site-specific development and refinement of these frameworks. Finally, our models capture successional pathways and native plant communities from the past and present; invasive species, climate change, and exotic plant pathogens are likely to alter future forest dynamics in novel and unpredictable ways. These models, however, provide us with baselines against which to interpret and assess the impacts of such effects on forest composition and processes.

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“…In late Holocene sites, N. menziesii pollen levels are either in trace amounts or its pollen is not recorded (McGlone, I 980;McGlone et al , 1988) Halocarpus is absent from Taranaki today but is found on the central North Island volcanic mountains (Atkinson,I 98 I) and in the Ruabine Ranges upper montane forest and subalpine shrubland (Elder,I965). The nearest locality today is c. 90 km from the Ararata Road Site.…”

Section: Biogeographymentioning

confidence: 99%

A late Pleistocene vegetational and climatic history of part oxygen isotope stage 5, Ararata, south Taranaki, New Zealand

Bussell¹

1993

Journal of the Royal Society of New Zealand

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A late Pleistocene palynological record of vegetation and climate is investigated from a 5m lignite section within terrestrial cover beds of the Ngarino Marine Terrace on Ararata Road, near Hawera, south Taranaki, New Zealand.The pollen assemblages are dominated throughout by high levels of pollen derived from gymnosperm trees. A lower zone (ARI) is characterised by high levels of pollen of Prumnopitys taxifolia, Libocedrus, shrubs and grass, interpreted to represent a stadia! phase with climate cooler and drier compared with present. A middle zone (AR2) is characterised by high levels of pollen of P. taxifolia, Dacrydium cupressinum, Metrosideros and spores of Cyathea dealbata-type and of the bryophyte Bryosporis anisopolaris Mildenhall and Bussell. Pollen values for Libocedrus and grass are low. These assemblages are similar to Holocene pollen spectra in the region but differ in containing high levels of Dracophyllum-type and Restionaceae pollen, and Gleichenia spores. The zone also lacks any significant levels of Ascarina lucida pollen, typical of interglacial maxima in this region, and is considered to represent an interstadial phase with climate approaching that of the present. The third zone (AR3) is characterised by high values for P. taxifolia, Nothofagus, shrub, and grass pollen with decreases in abundance of D. cupressinum and Metrosideros pollen, and C. dealbata-type spores in particular. This zone is considered to represent a transitional cooling phase leading into a stadia! period. Climate was initially cooler and drier than present but may have become wetter later.The Ngarino Terrace marine deposits that underlie the section provide a maximum age constraint of c. 210,000 yr, while tephra within the lignite are estimated to age 70,000-110,000 yr, and amino acid racemisation dating of a wood sample in the lignite provides an age estimate of c. 80,000 ± 20,000 yr. The lower pollen zone (ARI) is correlated with stadial oxygen isotope substage 5d, the middle zone (AR2) is correlated with interstadial substage 5c, and the upper zone (AR3) is correlated with early stadia! substage 5b. Climate during oxygen isotope substage 5c is inferred closely to have approached interglacial conditions similar to those of the present day.Libocedrus, Nothofagus menziesii, Halocarpus, Dracophyllum-type, and Gleichenia are some taxa which were growing near the Ararata Road Site at various times during oxygen isotope stage 5, but which are either not found in Taranaki today or are mainly restricted to higher altitudes or local areas in Taranaki.

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The effect of recent volcanic events and climatic changes on the vegetation of Mt Egmont (Mt Taranaki), New Zealand

Cited by 52 publications

References 11 publications

Late Quaternary (post 28,000 year B.P.) tephrostratigraphy of northeast and central Taranaki, New Zealand

Late Quaternary (post 28,000 year B.P.) tephrostratigraphy of northeast and central Taranaki, New Zealand

New Zealand forest dynamics: a review of past and present vegetation responses to disturbance, and development of conceptual forest models

A late Pleistocene vegetational and climatic history of part oxygen isotope stage 5, Ararata, south Taranaki, New Zealand

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