Relationships between volcanism and plate tectonics: A case-study from the Canterbury Basin, New Zealand

Barrier, Andrea; Bischoff, Alan; Nicol, Andrew; Browne, Greg H.; Bassett, Kari N.

doi:10.1016/j.margeo.2020.106397

Cited by 10 publications

(9 citation statements)

References 81 publications

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“…<0.5 s TwT) or no infill (Figure 5). In addition to the horst blocks, large composite volcanoes >10 km diameter also formed paleo‐highs in the Late Cretaceous post‐rift sequence which were not covered with sediment until the Latest Cretaceous or Paleocene (Figure 4b; Barrier et al., 2021; Bischoff et al., 2020).…”

Section: Results and Observationsmentioning

confidence: 99%

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Sedimentary architecture of a Late Cretaceous under‐filled rift basin, Canterbury Basin, New Zealand

et al. 2021

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The Canterbury Basin in southeastern Zealandia was initiated during the late Albian (ca. 105 Ma) as a rift system, prior to the onset of seafloor spreading between Zealandia and eastern Gondwana at ca. 85 Ma. Basin‐fill architecture and sediment types have been determined from interpretation of 2D and 3D seismic‐reflection lines tied to five wells and compared to outcrop data from the literature. These data show that Cretaceous syn‐rift basin‐fill architecture was controlled by normal faulting, which produced basin and range topography that persisted for more that ca. 30 Myr after the cessation of faulting. Initial sedimentation was dominated by short drainage systems sourced from within the basin to produce alluvial fans along fault scarps, which inter‐fingered with axial‐flowing braided river conglomerates, coal measures and mudstone‐rich lake deposits in more central portions of the basins. Marine incursion of the basin from the east commenced during rifting and onset of Gondwana breakup, with maximum water depths achieved in the Oligocene. Post‐rifting, detrital sediments were mainly sourced locally from structural highs and augmented by pelagic sedimentation, which collectively draped and eventually buried most of the earlier‐formed horsts by the Early Eocene. The temporal persistence of basin and range topography reflected the low rates of erosion of horst blocks compared to the rates of fault displacement. The lack of substantial sediment input from outside of the rift basin was a key factor in the under‐filling of the Canterbury Basin. This research emphasises the key role played by sediment supply in rift basin filling. Despite an abundance of active faulting at initiation, some rift basins may fill slowly over tens of million years after rift cessation.

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Section: Results and Observationsmentioning

confidence: 99%

“…However, other sources of sediments existed and comprised some of the main un‐buried horst structures (e.g. Caravel, Wherry highs) and large polygenic Late Cretaceous volcanoes located up‐dip from the shelf‐edge clinoform (Barrier et al., 2021; Bischoff et al., 2020).…”

Section: Results and Observationsmentioning

confidence: 99%

Sedimentary architecture of a Late Cretaceous under‐filled rift basin, Canterbury Basin, New Zealand

et al. 2021

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“…Similar evidence on the detailed imaging of plumbing systems is discussed with examples from the southeast Australian Margin and the Faroe‐Shetland region (McLean et al, 2017; Niyazi, Eruteya, et al, 2021; Niyazi et al, 2021). Accounting for the position of the sills in relation with the volcanic edifice and any controls from structural inheritance (Barrier et al, 2021; McLean et al, 2017; Niyazi, Warne, et al, 2021), these igneous features are interpreted to be associated with underlying syn‐rift faults; these faults probably acted as conduits for magma ascension to its final position within a pre‐volcanic sequence (dominantly unit 5b) and in some cases, extruding to surface and contributing to the build‐up of the volcanic edifice (Figure 4). Another relevant aspect of sills in the vicinity of the ESI is the similarity to what is observed around the Sintra massif (Figure 6d,e) (Alves, 1964; Ramalho et al, 1993; Sparks & Wadge, 1975).…”

Section: Discussionmentioning

confidence: 99%

Nature, timing and magnitude of buried Late Cretaceous magmatism on the central West Iberian Margin

et al. 2021

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The magma‐poor West Iberian Margin (WIM), as part of the Peri‐Atlantic alkaline province, records multiple evidence for intra‐plate post‐rift magmatism. Based on high‐resolution multichannel seismic data, this work discusses the presence of large volcanic and intrusive features in the Estremadura Spur, providing evidence for important magmatic activity during the drifting of the continental margin. Our observations reveal distinct voluminous fissure‐fed effusive sequences and the details of the 2800 m‐high Fontanelas compound volcano, including its external and internal architecture, secondary vents and associated lava flows, all of which were probably extruded at intermediate water depths. Numerous and morphologically diverse sills and sill complexes are also described, attesting to the presence of a Late Cretaceous shallow magmatic plumbing system in the area. Magmatism in this region is interpreted as having occurred during two main pulses and types of activity: (1) Coniacian to lower Campanian(?) age, characterised by fissural and fault‐controlled volcanism, which mostly extruded massive lobate/sheet lava flows; and (2) a second voluminous intrusive and extrusive event of mid to late Campanian age, which includes the intrusion of the Estremadura Spur laccolith and the prominent Fontanelas compound volcano with associated dendritic lava flows. The inferred volumes of the first fissure‐fed effusive event suggest a large eruption magnitude, comparable to some of the largest historical effusive eruptions. The second magmatic pulse led to the emplacement of discrete clusters of sills and sill complexes, as well as the construction of the ca. 2.8‐km‐high Fontanelas volcano, suggesting a syn‐rift structural inheritance that controlled the location of the Estremadura Spur Intrusion and the Fontanelas volcanic area. Altogether, a total volume of rock exceeding 1.452 km3 is estimated to have been emplaced or extruded in this region in a relatively short period, attesting to the prominence of the magmatism in this sector of the WIM.

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“…Previous studies have divided the igneous activity across New Zealand into four stages that corresponded to different tectonic periods (e.g. Barrier et al, 2021; Bischoff et al, 2020). For example, syn‐rift volcanism (105–83 Ma) associated with lithospheric thinning and rifting caused by the break‐up of Gondwana is observed across the Canterbury Basin (e.g.…”

Section: Geological Settingmentioning

confidence: 99%

Reutilization of fluid flow pathways over 54 million years, offshore New Zealand

2023

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Structures that facilitate fluid migration are common in sedimentary basins. We document several possible hydrothermal and/or volcanic vents located above a >157 km2, late Cretaceous volcanic field in the Great South Basin, offshore New Zealand. Three of the four vents are vertically stacked, suggesting episodic re‐use of the same fluid pathway between ca. 75 and 56 Ma. A palaeo‐pockmark dated to ca. 49 Ma and free gas occurring within strata ca. 21 Myr old are located directly above these stacked vents. The spatial association of the vents, pockmark and free gas further suggests re‐use of the fluid migration pathway(s) extended for over 54 Myr. Our results imply that reutilization of fluid flow pathways can affect the distribution of fluids within basins over prolonged periods, potentially impacting hydrocarbon/geothermal exploration and geohazard assessment.

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Relationships between volcanism and plate tectonics: A case-study from the Canterbury Basin, New Zealand

Cited by 10 publications

References 81 publications

Sedimentary architecture of a Late Cretaceous under‐filled rift basin, Canterbury Basin, New Zealand

Sedimentary architecture of a Late Cretaceous under‐filled rift basin, Canterbury Basin, New Zealand

Nature, timing and magnitude of buried Late Cretaceous magmatism on the central West Iberian Margin

Reutilization of fluid flow pathways over 54 million years, offshore New Zealand

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