Large volumes of magma emplaced and deposited within sedimentary basins can have an impact on the architecture and geological evolution of these basins. Over the last decade, continuous improvement in techniques such as seismic volcano-stratigraphy and 3D visualisation of igneous bodies has helped increase knowledge about the architecture of volcanic systems buried in sedimentary basins. Here, we present the complete architecture of the Maahunui Volcanic System (MVS), a middle Miocene monogenetic volcanic field now buried in the offshore Canterbury Basin, South Island of New Zealand. We show the location, geometry, size, and stratigraphic relationships between 25 main intrusive, extrusive and sedimentary architectural elements, in a comprehensive volcano-stratigraphic framework that explains the evolution of the MVS from emplacement to complete burial in the host sedimentary basin. Understanding the relationships between these diverse architectural elements allows us to reconstruct the complete architecture of the MVS, including its shallow (<3 km) plumbing system, the morphology of the volcanoes, and their impact in the host sedimentary basin during their burial. The plumbing system of the MVS comprises saucer-shaped sills, dikes and sill swarms, minor stocks and laccoliths, and pre-eruptive strata deformed by intrusions. The eruptive and associated sedimentary architectural elements define the morphology of volcanoes in the MVS, which comprise deep-water equivalents of crater and cone-type volcanoes. After volcanism ceased, the process of degradation and burial of volcanic edifices formed sedimentary architectural elements such as inter-cone plains, epiclastic plumes, and canyons. Insights from the architecture of the MVS can be used to explore for natural resources such as hydrocarbons, geothermal energy and minerals in buried and active volcanic systems elsewhere.
Volcanoes buried in sedimentary basins typically form complex magmatic-sedimentary systems [1, 2, 3, 4, 5, 6]. The large-scale architecture of buried volcanoes can be broadly divided into two realms: endogenous and exogenous. In the endogenous realm, magma emplaced within sedimentary strata can form a variety of intrusive bodies, each with different morphologies, sizes and contact relationships with the host rocks, typically controlled by the equilibrium between magma pressure and lithostatic pressure [7, 8, 9, 10]. In contrast, magma that reaches the Earths’ surface (the exogenous realm) typically produces diverse terrestrial and subaqueous morphologies, which are defined by the interplay of dynamic processes, such as eruptive styles, edifice growth mechanisms, magma composition, the nature of the eruptive environment, and tectonic settings [11, 12, 13, 14, 15].
The multitude of intrusive, eruptive and sedimentary bodies present in buried volcanoes can complicate their architectural characterisation [4, 6, 16, 17, 18, 19, 20]. Studies that describe the morphology (the form) and architecture (the arrangement of the parts) of monogenetic volcanoes are well constrained from the interpretation of modern and ancient outcropping systems [11, 13, 21, 22, 23, 24, 25]. However, complete architectural characterisation based on outcrop observations of both endogenous and exogenous parts of monogenetic fields are only possible in rare exhumed volcanic fields [26, 27]. This is especially true for the deep diatreme zones that lay beneath small volume maar volcanoes [28, 29]. Therefore, significant research is necessary to understand the key processes that collectively control volcanic and sub-volcanic architecture. High-quality 2D and 3D seismic surveys can provide a valuable opportunity to observe buried volcanic systems on outcrop to regional seismic scales [5, 15, 30, 31]. This approach can be enriched
by coupling the seismic data with information from borehole samples, wireline data, and laboratory experiments [3, 32]. Currently, few studies have been conducted aiming to characterise the complete architecture of buried monogenetic volcanic systems, including their plumbing system, eruptive deposits, and the sedimentary strata that enclose them [33, 34]. Here, we adapt the approach presented in  for characterizing the architecture of poly-genetic buried volcanic systems to unravel the complete architecture of the Maahunui Volcanic System (MVS), a submarine monogenetic volcanic field currently buried ca 1000min the offshore Canterbury Basin, New Zealand  (Figure 1). Interpretation of the diverse parts that together comprise the architecture of buried volcanic systems can provide valuable insights into how these ancient volcanoes formed and evolved in time and space [15, 36]. Understanding the complete architecture of volcanic systems is beneficial for estimating the potential of buried and modern volcanoes to host natural resources such as petroleum, geothermal energy and minerals [4, 37, 39, 40]. Insights of this workinto the exploration of geoenergy resources such as oil, gas and geothermal heat is the topic of further work to be publish as a separate paper.
The Maahunui Volcanic System (MVS) comprises a cluster of at least 31 middle Miocene small-volume (ca 1 km3) volcanoes currently buried by ca 1000 m of sedimentary strata in the Canterbury Basin, New Zealand  (Figure 1 and 2). During the Cenozoic, the Canterbury Basin experienced widespread and long-lived intraplate volcanism semi-continuously [41, 42, 43, 44, 45, 46, 47, 48, 49, 50] Products of this magmatism are primarily mafic in composition and resulted in the formation of both monogenetic volcanic fields such as the Waiareka/Deborah and Waipiata Volcanic Fields [44, 47], and large polygenetic volcanic complexes like those of Banks and Otago Peninsulas [45, 51]. In the offshore Canterbury Basin, several late Cretaceous to Pleistocene buried volcanoes and intrusive bodies have been mapped based on interpretation of 2D and 3D seismic reflection datasets [46, 52, 53, 54]. Despite a number of exploration boreholes that have recovered representative rocks of these buried offshore volcanoes, there has been few detailed studies of their eruptive histories.
Volcanoes of the MVS were imaged by high-quality 2D seismic lines and drilled by the Resolution-1 petroleum exploration well (Figure 1), which recovered a monzogabbro intrusion and correlative middle Miocene volcaniclastic rocks  (Figure 3). Volcanism in the MVS is estimated to have been active from12.7 to 11.5Ma. The products of this volcanic activity are observed over an area of ca 1,520 km2, located 40 km SW and offshore of Banks Peninsula (Figure 1). Eruptions in the MVS were short-lived and entirely submarine (500 to 1500 m in depth), controlled by a plumbing system that fed magma to disperse eruptive centres, which is common characteristic of monogenetic volcanic fields . The magmatic products of MVS melts are primarily basaltic-alkaline in composition, and mainly produced the deep-water equivalents of tuff cones and maar-diatreme volcanoes [35, 38] (Figure 3). After volcanism ceased, volcanoes located in a bathyal setting were buried and well preserved in the Canterbury Basin sedimentary strata, while higher volcanoes (> 200 m) located in a neritic setting were emergent at the paleo sea-surface and thus have had their tops flattened by erosional processes . These particular eruptive styles and differential erosion produced a variety of architectural elements related with the evolution of the MVS, which is the topic of the present paper.
In this study, we used more than 40,000 km of high-quality 2D seismic lines tied to six boreholes drilled in the northern Canterbury Basin (Leeston-1, Clipper-1, Ealing-1, Resolution-1; Charteris Bay-1 and -2) to interpret how diverse architectural elements vary in time and space in the MVS (Figure 1). We contrast the observations from this dataset with insights from tens of outcropping, submerged, and buried volcanic systems imaged by 3D seismic surveys from both New Zealand sedimentary basins and globally. The compiled datasets are complementary, providing information about the rock-types, eruptive styles, magmasediment interactions, volcanic morphologies, and volcanic architecture within the basin strata. The available information helps us to build a comprehensive volcanostratigraphic framework (Figure 4) showing the locations of individual, or sets of, cogenetic volcanic and sedimentary architectural elements, as well as explaining the complete architecture of the MVS from emplacement to burial in the Canterbury Basin.
The volcanic system concept applied in this work is an extension of the igneous boundaries of the Maahunui Volcanic Field (MVF) presented in [35, 38, 40]. In addition to the intrusive and extrusive parts of the MVF, the MVS includes two supplementary parts: i) the sedimentary strata deformed by the MVF plumbing system, and ii) the post-eruptive sedimentary deposits impacted by the presence of the MVF volcanoes (Figure 4).
Standard methods for analysing the stratigraphic record of sedimentary basins are typically based on observations of stratigraphic surfaces that represent shifts in the local architecture of the basin [55, 56, 57, 58]. Similarly, the magmatic-stratigraphy framework of MVS was also built following sequence stratigraphic principles such as stratal reflection relationships and depositional trends within seismic facies [59, 60]. In sedimentary basins impacted by igneous activity, these stratigraphic trends typically mark the boundaries between diverse magmatic events [2, 3, 6]. In this study,we use a model-independent sequence stratigraphic methodology [60, 61] to identify the bounding surfaces that mark important shifts in basin stratal patterns of the study area and the relationship of these bonding surfaces with the magmatic activity of the MVS.
We subdivide the stratigraphic record of the MVS into three first-order intervals (i.e. pre, syn and post-magmatic sequences; Figure 4). The pre-magmatic sequence predates magmatism and is cross-cut by the MVS plumbing system. The syn-magmatic sequence comprises both intrusive and extrusive parts of the volcano. The post-magmatic sequence is characterised by degradation and burial of the volcanic structures after magmatism has ceased. These first-order sequences were sub-divided into second-order magmatic stages (i.e. emplacement, construction, degradation and burial stages), depending on the dominant igneous or sedimentary processes that control the architecture of the north Canterbury Basin at each magmatic stage (Figure 4).
Definition of the primary magmatic-stratigraphic surfaces of the MVS follows well-established terminology such as, pre-eruptive surface (PrErS) and post-eruptive surface (PoErS). In other cases,we introduce new terminology such as syn-intrusive surface (SyInS), post-degradational surface (PoDgS) and post-burial surface (PoBuS). Further work is necessary to understand how the stratigraphic units of buried volcanic systems correlate with general models of volcanic stratigraphy proposed from outcropping and modern volcanoes [22, 62, 63, 64, 65, 66, 67]. Table 1 shows the characteristics of the stratigraphic surfaces and their correlative magmatic sequences and stages in the MVS.
|Stratigraphic surface||Abbr.||Contact relationship||Defined by||Relative time||Typical architectural elements|
|Post-burial surface||PoBuS||Conformable to both degradational and constructional stages.||Arbitrary surface that limits the relative influence of MVS in the basin architecture.||Can be synchronous or strongly diachronous (> 5 Ma) from diverse eruptive centres.||Top of the burial dome and associated seamount-edge fans.|
|Post- degradational surface||PoDgS||Erosional into constructional stage. Laterally conformable within burial stage.||Arbitrary surface relative to one or more eruption centres, for which the rate of burial exceeds the rate of degradation.||Can be synchronous or diachronous from diverse eruptive centres (> 1 Ma and < 2 Ma).||Epiclastic debris deposits proximal to volcanic edifices and distal non-volcanogenic sedimentary deposits. Canyons and gullies,|
|Post-eruptive surface||PoErS||Overlies the constructional stage. Amalgamated or parallel with the PrErS for increasing distance from eruptive centres.||Younger eruptive event in MVS.||Minor diachronous from diverse eruptive centres. Usually < 1 Ma. Max 1.5 Ma.||inter-cone plains. Epiclastic debris deposits proximal to volcanic edifices and distal non-volcanogenic sedimentary deposits that overlay PoErS.|
|Pre-eruptive surface||PrErS||Overlies the pre-magmatic sequence and the emplacement stage.||Older eruptive event in MVS.||Minor diachronous from diverse eruptive centres. Usually < 1 Ma. Max 1.5 Ma.||Primary eruptive and eruption-related deposits that overlay PrErS.|
|Syn-intrusive surface||SyInS||Cross-cut the pre-magmatic sequence. Eventual minor cross-cutting into the constructional stage near eruptive centres or at very shallow intrusions.||Presence of intrusive bodies and strata deformed by magmatism.||Minor diachronous from diverse eruptive centres. Usually < 1 Ma. Max 1.5 Ma.||Dikes, sills, laccoliths, stocks, saucer-shaped sills, and disrupted blocks.|
Each of the MVS magmatic stages is characterised by a network of genetically related fundamental building blocks (i.e. architectural elements), formed by interactions between intrusions, eruptions, and sedimentation. The concept of architectural elements was introduced by  and extended  to describe sets of genetically related rock associations that form the fundamental building blocks of fluvial systems. This concept is now widely used in most clastic sedimentary systems [70, 71, 72, 73, 74, 75, 76, 77], and has also been successfully introduced in carbonate systems (e.g. [78, 79, 80]. In this study, the architectural element concept is applied to document the fundamental blocks of volcanic systems buried in sedimentary basins .
Interpretation of the architectural elements of the MVS was primarily achieved by observations from 2D seismic lines that image the volcanic field, and follows two approaches: one with complementary information from well data, the second without well data (Figure 5). In both approaches, we initially characterised the 2D aspects of seismic anomalies that correspond to igneous rocks buried in the study area. This characterisation was based on numerous criteria such as, the morphology of igneous seismic anomalies, their internal and external seismic facies, and their stratal relationship with enclosing strata. Additional criteria includes the type of stratigraphic surface that bounds the seismic anomaly from adjacent strata, in other words, the stratigraphic position of the anomaly in the volcano-stratigraphic framework (Figure 4).
The results from 2D characterisation were compared with observations from outcropping and buried analogues elsewhere, searching for insights into possible 3D architectures that may correspond to the seismic anomalies identified in 2D seismic data. The final interpretations produced similar results whether the seismic data was correlated to drillholes or not. However, rock samples from drill holes are advantageous because they can provide physical evidence of the subsurface rocks imaged indirectly by remote sensing techniques (Figure 5). The utility of 2D seismic reflection methods are limited by their resolution and line spacing, which in the study area are tens of meters vertically and <1 km laterally.
We have identified 25 architectural elements that together comprise the complete architecture of the MVS (Figure 6). In this section we present a detailed characterisation of each architectural element according to their stratigraphic position in the pre-, syn- and post-magmatic sequences. Architectural elements formed during the pre-magmatic sequence and undeformed by magmatic processes are not described in this work.
The syn-magmatic sequence of the MVS comprises the endogenous and exogenous parts of the volcanic system. This sequence is characterised by rock units formed during the emplacement of intrusive bodies, eruptions, and time-equivalent sedimentation and, also, encompasses pre-magmatic strata deformed by magmatic activity (Figure 6).
The syn-intrusive architectural elements of the MVS were formed in association with the emplacement of a shallow (<3 km) magmatic plumbing system that intruded and deformed the Cretaceous to Miocene sedimentary strata of the northern Canterbury Basin (Figures 1 and 6). Synintrusive architectural elements of the MVS comprise sills, saucer-shaped sills, dikes, small stocks and laccoliths. These syn-intrusive elements typically occur below the PrErS surface, however, some shallow intrusions cross-cut and emplaced within syn-eruptive deposits near eruptive centres (Figures 6, 7 and 8). Together, the syn-intrusive architectural elements display characteristic geometries and relationships with enclosing strata,which are discussed in the next section. Table 2 shows the main characteristics of the syn-intrusive architectural elements of the MVS.
|Element||Association||Seismic facies||Bounding surfaces||Geometry||Indicative process|
|Sills||Plumbing-types 2 and 4.||Anomalous single, high amplitude semi-continuous horizontal reflector.||Sharp contact between single high amplitude reflector and external bedded seismic facies.||Tabular horizontal to sub-horizontal.||Dense rock body emplaced parallel within enclosing strata.|
|Saucer-shaped sills||Plumbing-type 1 and 2.||Typically single high amplitude, semi-continuous, horizontal to inclined reflector.||Sharp contact between single high amplitude reflector and external bedded seismic facies.||Saucer-like.||Dense rock body emplaced parallel within enclosing strata. Jack-up, brittle deformation and body cross-cutting enclosing strata.|
|Dikes||Plumbing-types 3, 4 and 5.||Single, narrow, vertical to sub-vertical transparent (i.e. reflector-free) discontinuities in bedded strata.||Sharp contact between sub-vertical transparent discontinuities and external bedded seismic facies.||Tabular vertical to sub-vertical. Typically seismically unresolved.||Rock body cross-cutting enclosing strata.|
|Dikes-and- sills swarm||Plumbing-types 2, 3 and 4.||Multiple high amplitude, discontinuous, horizontal to steeply inclined reflectors in chaotic configuration.||Sharp contacts between multiple, chaotic, high amplitude reflectors and external bedded seismic facies.||Complex, chaotic.||Multiple rock bodies cross-cutting and parallel emplacing within bedded strata.|
|Stocks and laccoliths||Plumbing-types 2 and 3.||Single, thick, high amplitude, typically continuous, semi-circular reflector.||Sharp contacts between high amplitude reflectors and external seismic facies.||Sub-geoidal. Not always resolved in seismic data.||Rock body cross-cutting enclosing strata.|
|Disrupted blocks||Plumbing-types 1, 2, 3, 4 and 5.||Multiple narrow, vertical to sub-vertical transparent discontinuities in bedded strata.||Sharp contact between sub-vertical transparent discontinuities and external bedded seismic facies.||Chaotic.||Brittle deformation of bedded strata.|
|Jacked-up domes||Plumbing-types 1, 2, and 3.||Bedded strata domed above typically single high amplitude, semi-continuous, horizontal to inclined reflector.||Gradational contact between domed and parallel bedded seismic facies.||Downward- concave dome.||Strata jacked up above rock body emplaced parallel within enclosing strata.|
We broadly characterise the shallow plumbing system of the MVS into five plumbing-types (Figures 6, 7 and 8), based on the geometry, size and depth of the intrusive bodies, and on their relationship with the enclosing sedimentary strata. Each plumbing-type can contain a variety of intrusive bodies such as dikes, sills and stocks, which are individually described later in this section.
Plumbing-type 1 comprises large (up to 5 km in width and ca 100mthick) sills and saucer-shaped intrusions emplaced into the lower Cretaceous-Paleocene sequences of the northern Canterbury Basin (500 to 1000 m deep at the time of the formation of these intrusions). The relationship of these bodies display an intrusive network with minor branching, and extensive lateral migration of magma, up to 5 km from the extremities of the saucer-sills (Figures 6, 7 and 8).
Plumbing-type 2 is characterized by small (<1 km in width and <100 m thick), disrupted, parallel, transgressive or saucer-shaped intrusions emplaced into Cretaceous to Oligocene strata (Figures 6, 7 and 8). Typically, these bodies show a complex intrusive network, intense lateral and vertical branching, and moderate magma lateral migration (up to 1 km).
Plumbing-type 3 displays narrow, steeply inclined and discontinuous conduit zones, located immediately above the tips of the large saucer-shaped intrusions of plumbing-type 1 (Figures 6, 7 and 8). These bodies have a complex intrusive network characterised by intense vertical branching, and little lateral migration of magma (<200 m).
Plumbing-type 4 comprises shallow (up to 250 m deep) swarms of narrow, steeply inclined, parallel and transgressive intrusions, located immediately below eruptive vents (Figures 6, 7 and 8). These bodies display a complex intrusive network with numerous branches, and little lateral migration of magma (<300 m).
Plumbing-type 5 are narrow (<50 m in width) and steeply inclined conduit zones showing simple intrusive network, little branching, and little lateral migration of magma (<50 m). These bodies form a single and continuous intrusion zone that cross-cuts the basement fabric and the Cretaceous-Miocene sequences of the northern Canterbury Basin (>5 km, which is the resolution limit of our dataset). Its upper termination is connected with the root zone of some MVS eruptive vents (Figures 6, 7 and 8).
Sills and saucer-shaped sills are the most common syn-intrusive architectural element seismically imaged in the MVS (Figures 3, 5, 6, 7 and 8). In seismic lines, sills and saucer-shaped sills occur between 1.1 and 1.8 sec TWT (ca 500 to 1000 m at the emplacement time), and often intrude paralic to marine Cretaceous-Paleocene sedimentary strata. Individual or sets of tabular, parallel, transgressive and saucer-shaped sills vary in width from a few hundred meters to 5 km and ca 100 m in thick (Figure 3). The presence of intrusions is often associated with disrupted and deformed enclosing sedimentary rocks, demonstrating that magma being emplaced into, or moving through, the sedimentary basin can produce kilometre-scale deformation. Magmatic-related deformation can include folds, jacked-up strata, and both reverse and normal faults (Figures 3 and 7). These interpretations are supported by observations from sedimentary basins elsewhere [4, 6, 27, 34, 50, 52, 81, 82, 83, 84, 85] and also by laboratory experiments [36, 86].
Petrographic analyses of a Type-1 saucer-shaped sill recovered from the Resolution-1 well provides evidence that this plumbing-type has emplaced and crystallized at relatively shallow depths ca 950 m in the basin  (Figure 3). Seismic images show a direct connection between saucersills and numerous MVS eruptive vents (Figure 7), suggesting that these intrusions likely have served as stationary magma chambers to fed eruptions at the middle Miocene paleo-submarine seabed . This relationship between the emplacement of shallow sills and eruptions was previously described in several locations globally, including buried examples in southern Australian [4, 20], and North Sea sedimentary basins [34, 81, 83], and also from outcrops such as those from the Hopi Buttes Volcanic Field,USA and the Pannonian Basin, western Hungary .
Dikes and other potential magmatic conduits are syn-intrusive architectural elements characterised by vertical and sub-vertical igneous bodies emplaced beneath the pre-and post-eruptive surfaces (Figures 6, 7 and 8). Due to their steep inclination and narrow lateral thickness, dikes and other magmatic conduits are typically seismically unresolvable. We recognise these bodies by narrow, steeply inclined, tabular high-amplitude reflectors, and by sub-vertical discontinuities that crosscut pre-magmatic sedimentary strata (Figure 8). In the MVS, these intrusions commonly form complex branching networks, in association with sills and stocks of the plumbing-types 2, 3 and 4, which form similar networks as dikes and sills mapped from 3D seismic reflection data in the Ben Nevis mono-genetic volcanic field, for example . In other cases, we observe narrow sub-vertical discontinuities in host strata that can be tracked from MVS eruptive centres to depths of at least 5 km (plumbing-type 5). Because these sub-vertical discontinuities do not show branching or lateral migration, they could potentially represent simpler source-to-surface magmatic pathways from deeper magma chambers .
An analogy for dikes in the MVS is provided by a network of dikes and sills intruding poorly indurated Eocene marine strata in the inland Canterbury Basin (Figure 9). These intrusions show distinctive outcrop patterns that are dependent on their emplacement depths. Deeper level intrusions mainly comprise sub-vertical dikes that show sharp contact relationships with the host sandstones. Shallower intrusions have magma-finger terminations associated with thin (<1 m) sill apophyses and peperitic borders. Tens of meters up-sequence (and above the intrusions), calcite veins occur cross-cutting sedimentary strata in the absence of hypabyssal rocks, suggesting migration of hydrothermal fluids above these intrusions. Magma finger structures are commonly interpreted to be emplaced within relatively soft sedimentary strata , but they have also been described emplaced into craters of maar-diatreme volcanoes [90, 91].
Disrupted blocks are recognised in 2D seismic lines by parallel reflectors with abrupt lateral discontinuities (Figures 8 and 10a and b). Disrupted blocks typically occur below eruptive centres and in association with plumbing-types 3, 4 and 5, or above and lateral to intrusive bodies of plumbing-types 1 and 2 (Figures 3, 7 and 8). These discontinuous rock masses were likely formed due to fracturing, faulting and forced-folding of host strata, to accommodate deformation caused by the emplacement of intrusive bodies [6, 82, 92]. Another possible mechanism that could form disruptive blocks is the emplacement of multiple closely-spaced intrusions, such as the field example from Banks Peninsula volcanoes shown in Figures 10C and D. Faulting of host sedimentary strata can be an important process for creating pathways for magma and/or fluid migration within basin strata [86, 93].
Jacked-up domes are formed by uplift of pre-eruptive sedimentary strata above large intrusions (Figures 3, 4, 7, 8, 10 and 11). In the study area, these dome structures vary in diameter from 1 to 5 km and commonly occur above large saucer-shaped sills (plumbing-type 1). Similar dome structures are described in magma rich sedimentary basins elsewhere, where they typically form in association with fracture networks containing both normal and reverse faults, which are often observed along the borders of domed structures [36, 81, 82, 86]. These fracture networks may provide conduits for magma and fluids as they ascend up-sequence (plumbing-type 3).
Regionally, the isochron map corresponding to the top of the early Miocene shows a semi-elliptical area of 1,137 km2 that contains several 4-way dipping structures with maximum vertical relief of ca 100 m, located above large saucer-shaped intrusions and/or dikes-and-sills swarms (Figure 11). A possible explanation for this regional uplift (which we refer to as the pre-eruptive dome) is that the large swarms of intrusions emplaced within the sedimentary basin may produce inflation and ground dilatation above the MVS plumbing system, similar to the dome beneath Kora volcano in New Zealand’s Taranaki Basin [6, 94, 95]. Another possible explanation is that the pre-eruptive dome could be formed by thermal uplift, representing a smaller-scale version of the Ethiopian and Kenya domes in the Eastern African Rifts [96, 97, 98].
Seismic anomalies associated with plumbing-types 2 and 3 have high amplitude reflectors with irregular and concave downward shapes (Figure 8). These anomalies cross-cut deformed enclosing strata, typically producing a domed-shaped geometry above these intrusions. These bodies have been interpreted to represent small (<200 m) stocks that intruded pre-magmatic sedimentary sequences. Laccoliths possibly occur in plumbing-types 2 and 3, however, separating them from stocks is not possible due to the kilometre-scale spacing of our seismic lines.
In summary, the plumbing system of the MVS is characterised by a complex network of sills and dikes that deform pre-magmatic sedimentary strata. Many of these intrusions (i.e. large saucer-shaped sills of plumbing-type 1) served as stationary shallow (<1 km) magmatic chambers that fed eruptions at the middle Miocene seabed. In other examples, a deeper source-to-surface system (plumbing-type 5) is likely to have fed some of the MVF volcanoes. Interpretation of the MVS plumbing system suggests that a significant volume of magma (ca 50 km3) was emplaced within the sedimentary strata of the basin, with a much smaller volume (ca 20 km3) reaching the paleo-seabed .
Syn-eruptive architectural elements are cogenetic sets of eruptive, eruption-related and time-equivalent non-volcanogenic sedimentary rock units formed during the active constructional stage of the MVS (Figure 6). During the constructional stage, the architecture of the volcanoes in the MVS was mainly controlled by interactions between internally (i.e. magma composition, pressure and magma ascent rate), and externally (i.e. interaction with water and organic rich host rocks, soft or hard country rock, and the presence of pre-existing structures), driven mechanisms of fragmentation, dispersal and volcanic edifice growth [35, 38]. These processes controlling the morphology and architecture of volcanoes are commonly observed in active volcanoes and interpreted from ancient volcanic systems in outcrop [21, 25, 99, 100].
Two main volcano-type morphologies have been observed in the MVS seismic data: (i) crater-type and (ii) cone-type volcanoes. Each of these volcano-types contains distinctive combinations of cogenetic sets of syn-eruptive architectural elements at different scales, although some elements occur in both volcano-types (e.g. tephra fallout carpets). We have observed that the seismic morphology of these buried volcanoes is similar to subaerial and submarine monogenetic volcanoes well documented in the literature (e.g. [20, 21, 25, 28, 99, 101, 102, 103, 104, 105] (Figures 12 to 19). These similarities assist our interpretations and provide information to construct a comprehensive time-space framework showing the distribution of architectural elements for each volcano-type.
Crater-type volcanoes of the MVS are interpreted to represent the deep-water equivalent of maar-diatreme volcanoes. In seismic reflection imagery, crater-type volcanoes are characterised by funnel and basin-like excavations into pre-magmatic sedimentary strata. Reconstructed MVS diatremes vary in diameter from 900 to 1700 m, and are excavated 90 to 230mdeep into the PrErS . These craters were formed in relatively soft ground, locally corresponding to the bathyal Tokama Siltstone in the upper part, and to the micritic Amuri Limestone and Ashley Mudstone in the root zone (Figures 12 and 13). Basin-like excavations are rare in the MVS and difficult to characterise due to seismic resolution limitations, thus, further descriptions consider only morphological aspects of funnel-like morphologies.
The architecture of MVS crater-type volcanoes can be divided into eight distinctive fundamental architectural elements: (1) root zone, (2) lower and (3) upper diatreme, (4) tephra ring, (5) ring plain, (6) intra-crater cones, (7) overspill wedge and (8) tephra fallout carpet (Figures 12 to 14). The main characteristics of these crater-type volcanoes are presented in Table 3.
|Element||Location||Seismic facies||Bounding surfaces||Geometry||Indicative processes|
|Root zone||Bottom of the funnel-like structure.||Moderate to high amplitude and disrupted reflectors showing depression towards the centre of the structure.||Seismically unresolved.||Unsure, probably geoidal.||Brittle deformation. Post-eruptive subsidence?|
|Lower diatreme||Centre of the funnel-like structure.||Moderate amplitude, discontinuous and chaotic reflectors.||Sharp contact between internal unbedded seismic facies from external bedded reflectors.||Funnel-like.||Brittle deformation. Excavation into PrErS. Intense fragmentation and dispersion of material.|
|Upper diatreme||Top of the funnel-like structure.||Moderate amplitude, semi-continuous, parallel and sub-horizontal reflectors.||Sharp contact between Internal bedded seismic facies from external unbedded seismic facies below, and mound-like facies above.||Funnel- like.||Deposition of layered material into an upper crater.|
|Tephra ring||Symmetrically lateral to the upper diatreme.||Single high amplitude, continuous and inclined reflectors in A shape.||Sharp contacts between the upper and lower limits of the high amplitude reflector. Laterally gradational to facies of the ring plain.||Ring-like.||Deposition of “hard” material in relatively steep repose angle near a vent zone.|
|Ring plain||Symmetrically lateral to the tephra ring.||Single high amplitude, continuous, parallel and sub-horizontal reflectors.||Sharp contacts between upper and lower limits of the high amplitude reflector. Laterally gradational to facies of the ring plain. Fade with increasing distance from the vent zone.||Circular tabular, thinner with increasing distance from the vent.||Intense fragmentation and dispersion of material ejected from the diatreme. Deposit parallel to basin sediments immediately above PrErS.|
|Intra-crater cones||Above of the funnel-like structure.||Moderate amplitude reflector with mound-like shape and transparent internal seismic facies.||Sharp contacts between the upper and lower limits of the mound-like structure and external bedded facies.||Mound-like and possible small cone-like.||Deposition of material above the upper diatreme. Late eruptive events?|
|Overspill wedge||Symmetrically lateral to the intra-crater cones.||High-to-low amplitude, discontinuous reflectors that together show a wedge shape.||Sharp contacts between upper and lower limits of the wedge-like structure. Fade with increasing distance from the vent zone.||Circular wedge-like.||Material that overspill the tephra ring and deposit parallel to basin sediments immediately above the ring plain.|
|Tephra fallout carpet||Seismically unresolved, but probably distal to the funnel-like structure.||Seismically unresolved, but probably amalgamated with reflectors that represent basin sediments.||Seismically unresolved, but probably sharp and parallel contact between volcaniclastics and Tokama Siltstone (wire-logs of the Resolution-1)||Seismically unresolved, but probably tabular.||Probably represent thin and tabular layers of tephra interbedded with basin sediments.|
Based on the presence of disrupted reflectors showing minor depressions located at the base of the diatreme structures, we interpret that the bottom part of the crater-type volcanoes in the MVS contain a root zone (Figures 12 to 14). In the context of terrestrial maar-diatreme forming eruptions, the root zone is interpreted to be the locus of thermohydraulic explosions [21, 25, 28, 103], and likely contains minor syn-intrusive architectural elements such as contact breccias, disrupted pre-magmatic blocks, and late intrusive plugs [90, 91]. However, we do not recognise indicative seismic facies that could support the occurrence of these intrusive elements, probably because they are too small to be seismically resolved. In some examples, the possible location of a root zone is coherent with seismic reflectors that correspond to the Amuri and Omihi limestones, and possibly also to the Charteris Bay Sandstone in their deepest parts (Figures 12 and 14). The middle Miocene volcaniclastic rocks sampled in Resolution-1 contain numerous lithics of limestone and very-fine white sandstone , which are interpreted to provide evidence that the country rocks of the root zone have experienced intense fragmentation, and were incorporated into the material ejected by high energy explosive eruptions. In diatremes of the MVS, the depression at the centre of the funnel-like structure may indicate post-eruptive subsidence (Figures 12 and 14).
The lower diatreme comprises a zone with unbedded and chaotic structure below the PrErS (Figures 12 to 14), which suggest that these pre-magmatic sedimentary strata were deformed. The chaotic strata could indicate processes such as fracturing of the host rock due to shockwaves, crater-wall brecciation and blocks collapsing during large explosive activity [25, 28]. Another possible process responsible for the unbedded-chaotic seismic character of the lower diatreme zone is the formation of intra-diatreme faults, developed during post-eruptive subsidence [21, 28, 105]. The presence of feeder intrusions of plumbing-type 4 and 5 are likely to occur in the lower diatreme, supported by seismic images showing sub-vertical to sub-horizontal, moderate amplitude reflectors in association with disrupted pre-magmatic blocks (Figures 12 and 13). Intrusive bodies located in the lower part of maar-diatreme volcanoes are commonly observed in outcrops elsewhere [21, 25, 28, 90, 91].
The upper diatreme is located immediately above the lower diatreme (Figures 12 to 14). This architectural element, in contrast to what is observed in the lower diatreme, is characterised by a bedded structure, showing seismic reflectivity consistent with the presence of rock bodies deposited sub-horizontally. The seismic aspect of the upper diatreme suggests that this zone is composed of alternating layers, perhaps layers of tephra material sourced from late stage eruptions, together with possible slumps, slides and debris deposits that infill the top part of the diatreme (Figure 12 and 14). Similar stratigraphic relationships are typically observed in analogue diatremes elsewhere [21, 25, 28, 105].
Laterally and symmetrical to both sides of the diatreme, we observe a distinctive parallel and continuous high-amplitude reflector located immediately above the PrErS horizon (Figures 12 and 13), which we interpret to correspond to the tephra ring and ring plain a of a maar-diatreme volcano. Morphological and morphometric reconstruction of the MVS volcanoes suggest that these reflectors are inclined at ca 20∘ close to the vent zone . These reflectors become progressively sub-horizontal and parallel to basin strata reflectors with increasing distance from the vent. Their high-amplitude continuous seismic character ‘fades-out’ to become semi-continuous, moderate-to-low amplitude (this last, is the characteristic seismic facies of Tokama Siltstone; Figures 12 and 13). This ‘fading-out’ character of seismic reflectors with increasing distance from eruptive centres has been interpreted to mark the transition of volcanic to sedimentary rocks [2, 20, 53]. It is possible to map the lateral extentof the high-amplitude reflectors for ca 5 km on both sides of the diatreme structure, which suggests that these reflectors represent material dispersed from the vent zone, possibly formed by high energy explosive eruptions . Near to the diatreme zone, reflectors are steeply inclined and outward-dipping, suggesting that they were formed by accumulation of tephra ejected as ballistic material during pyroclastic eruptions (Figure 12 to 14).
In the study area, bedded diatremes are typically overlain by a dome- and cone-like seismic structure (Figure 12 and 13). These dome and cone morphologies are physically limited by the crater zone of the maar-diatreme volcanoes. Based on their convex upwards geometries, and used in conjunction with examples described in the literature [21, 25], we interpret these seismic facies to correspond to intra-crater cones formed by the accumulation of tephra near the eruptive vent. Minor hyaloclastite and pillow-lava material may also be deposited in the crater zone during late stage eruptions, however, we did not find diagnostic features that confirm their occurrence in the MVS.
Lateral to the intra-crater cone and overlying the tephra ring and plain, we observe a characteristic seismic facies composed of discontinuous moderate-amplitude reflectors, here referred to as the overspill wedge. As observed in the tephra ring and ring plain, reflectors of the overspill wedge merge and fade-out with increasing distance from the eruptive centre. This suggests that they were formed by material sourced from the diatreme zone, possibly by ballistics and other dispersal mechanisms related to submarine eruptive plumes (e.g. eruption-fed density currents,  (Figure 12 and 13). This wedgehas a maximum lateral extent of ca 7 km from both sides of the diatreme, with reconstructed vertical heights of ca 30 m . The overspill wedge may also contain minor pillow-lavas and hyaloclastite deposits , interbedded with deposits from explosive submarine eruptions. However, we did not identify seismic facies that could confirm the presence of lava-flow deposits in the overspill wedge, perhaps due to lack of seismic resolution.
The presence of thin tuffaceous layers interbedded with the Tokama Siltstone  suggests that tephra material could be transported and deposited kilometres from the MVS vents. Studies of submarine-eruption deposits show that material ejected into the water column can be transported by suspension for long distances (>100 km), to be deposited distal to the eruptive centre as thin and tabular tephra layers [99, 106, 107, 108, 109, 110, 111]. Based on this evidence, we infer the presence of a tephra fallout carpet occurring in distal parts of the maar-diatreme volcanoes (Figure 12 to 14), however, this architectural element cannot be directly seismically resolved.
Crater-type volcanoes of the MVS comprise syn-eruptive architectural elements that show deep craters excavated into the PrErS horizon, and associated deposits that indicate substantial material dispersed laterally from these craters. These observations collectively suggest that crater-type volcanoes were likely formed by high-energy explosive eruptions [28, 112, 113, 114], which are rarely interpreted to occur at water depths > 100 m [81, 115, 116, 117, 118, 119]. Detailed stratigraphic mapping coupled with information from the Resolution-1well provide strong evidence that some crater-type volcanoes of the MVS erupted in a subaqueous environment around 1000 m deep [35, 38]. The geometry and spatial arrangement of the architectural elements in the crater-type volcanoes suggest that funnel-like structures are likely to represent the deep-water equivalent of maar-diatreme, and basin-like structure possibly correlate with tuff rings volcanoes (Figure 3 and 13).
Cone-type volcanoes are interpreted to be the deep-water equivalent of tuff cones. In contrast to crater-type volcanoes, MVS cone-type volcanoes are characterised in seismic imagery by a sequence of reflectors that pile-up close to the vent zone, forming a convex-upwards curvature of the PoErS above the PrErS horizon with minor excavation into pre-eruptive strata (Figures 15, 16 and 19). This volcano-type more commonly occurs as isolated cones, typically ranging in size from 1 to 3 km in diameter, and 100 to 300min height . Seismic data show that the sub-vent zone of this volcano-type contains high-amplitude reflectors that may represent intrusions related to plumbing-types 3, 4 and 5 (Figure 8, 16 and 19). However, most MVS cone-type volcanoes appear to be fed by large sill intrusions related to plumbing-types 1 and 3. The exception is the overlapped volcanic cluster (Figure 8) that appears to be fed by plumbing-type 5, and does not show evidence that it is fed by a shallow (< 1 km) magmatic chamber.
The syn-eruptive architecture of the cone-type volcanoes of the MVS can be divided into five fundamental elements, based on distinctive seismic facies, and the surfaces that bound characteristic morphologies. These architectural elements are: (1) basal cone, (2) central crater, (3) tephra flank, (4) cone apron and (5) tephra fallout carpet (Figures 15 to 19). The main characteristics of the syn-eruptive architectural elements of this volcano-type are shown in Table 4.
|Element||Location||Seismic facies||Bounding surfaces||Geometry||Indicative processes|
|Basal cone||Bottom of the cone-like structure.||Moderate to high amplitude sub-horizontal and parallel reflectors.||Sharp to gradational contact between internal sub-horizontal and parallel facies, from external seismic facies with inclined, disrupted or chaotic reflectors||Unsure, probably tabular.||Material piled-up near vent, sub-parallel to basin sediments and above the PrErS.|
|Central crater or vent zone||Centre of the cone-like structure.||Typically transparent, but also show moderate to low amplitude, discontinuous, chaotic or parallel reflectors dipping inward the central crater.||Sharp to erosive contact between internal chaotic seismic facies from external facies typically bedded and inclined.||Probably cylindrical based in analogues.||Material disperse out of the crater zone. Chaotic deposits probably represent collapses of the crater walls, and deposition of intra-crater layers of tephra.|
|Tephra flank||Symmetrically lateral to the central crater.||Moderate to low amplitude, semi-continuous, parallel and inclined reflectors dipping outwards from the central crater zone.||Sharp to erosive contact between internal inclined and bedded seismic facies from external chaotic (towards the central crater) or sub-parallel seismic facies (towards the basin).||Conical.||Deposition of layered material near a vent zone and above the basal cone, or above PrErS.|
|Cone apron||Symmetrically lateral to the tephra flank.||Low to high amplitude, typically continuous and sub-parallel and sub-horizontal reflectors.||Sharp to gradational between bedded seismic facies that pinch with increasing distance from the eruptive centre.||Ring-like.||Deposition of material distal to a vent zone and above PrErS|
|Tephra fallout carpet||Seismically unresolved, but probably distal to the funnel-like structure.||Seismically unresolved, but probably amalgamated with reflectors that represent basin sediments.||Seismically unresolved, but probably sharp and parallel contact between volcaniclastics and Tokama Siltstone (wire-logs of the Resolution-1)||Seismically unresolved, but probably tabular.||Probably represent thin and tabular layers of tephra interbedded with basin sediments.|
The basal cone is characterised by sub-horizontal and parallel reflectors of high- to moderate-amplitude that are located near the interpreted vent zone (Figure 15). The geometries and seismic characteristics of the basal cone comprise sets of stacked reflectors, suggesting deposition of alternating tephra layers and perhaps deposits such as subaqueous lavas and hyaloclastites formed during the initial eruptive stages of the cone construction (Figures 8, 15, 16 and 19). In addition, the presence of high-amplitude reflectors cross-cutting sub-horizontal reflectors may indicate that the basal cone also contains minor shallow intrusions of plumbing type-4 (Figure 8), which are commonly observed in monogenetic volcanoes elsewhere [25, 27, 34, 87, 88].
The central crater or vent zone is characterised by disrupted, chaotic and layered reflectors inwardly-dipping towards the centre of the cone structure (Figures 15, 16, 18 and 19), providing evidence that deposits locally infilled a negative shallow depression above the PrErS horizon. This architectural element is typically located overlying seismic facies that indicate the presence of magmatic conduits and intrusive bodies (i.e. disrupted pre-magmatic reflectors, high-amplitude reflectors cross-cutting enclosing strata), as shown by [6, 94, 95, 120] in buried volcanic systems elsewhere. The structure of the central crater shows only minor excavation into the PrErS horizon, which suggests that eruptions in cone-type volcanoes were much less damaging to the host rocks than what is observed in the crater-type volcanoes . We interpret this architectural element to have been formed by mechanisms such as jets of tephra, followed by reworking and deposition of material into the central crater. Outcrop observations of ancient volcanoes in the Waiareka-Deborah volcanic field, South Island of New Zealand, show that the crater zone of submarine monogenetic volcanoes typically contain massive, chaotic, to amalgamated deposits of lapilli-tuff to tuff-breccia, formed by tephra jets and ballistics during explosive eruptions, and deposits of tephra dipping inwards in the crater zone [101, 121, 122].
The tephra flank is characterised by inclined, low-to moderate-amplitude reflectors dipping outward from the centre of the cone-shaped structure (Figure 16). We interpret the flanks of MVS cone-type volcanoes to predominately contain fragmented material that originated from submarine pyroclastic eruptions, rather than subaqueous lava flow deposits. This interpretation is supported by: (i) a clear lateral relationship of the tephra flank with a crater (vent) zone that suggests explosive activity, (ii) seismic facies showing low- to moderate amplitude, semi-continuous, parallel and inclined reflectors, symmetrically dipping away from the vent zoneand, (iii) rock-types collected in the Resolution-1 well indicate explosivity in the MVS (peloidal fragments enveloped by palagonite films, broken crystals and relics of bubble walls; .However, some minor lavas and hyaloclastite deposits are commonly observed in explosive monogenetic volcanoes elsewhere . Thus, these lava deposits (and possibly also type-4 intrusions) are expected to occur in the tephra flank, which is suggested by localised and isolated high-amplitude reflectors. Deposits of the flanks of monogenetic submarine volcanoes are typically formed by eruption-fed density currents and comprise tabular, thinly-bedded layers of tephra dipping away from the vent zone, [101, 102, 121]. Eruption-fed density currents usually form well-sorted and thinly-bedded pyroclastic deposits similar to Td and Te turbidite facies of the Bouma sequence [99, 123]. These bedded tuffaceous rocks are possible lithofacies that may occur on the tephra flanks of MVS volcanoes (Figure 17).
The cone apron is characterised by sub-horizontal and parallel reflectors that pinch and amalgamate with basin reflectors as distance increases from the cone structure (Figures 15, 16 and 19). The Resolution-1 well penetrates the distal part of the cone apron of the volcano pc14 (Figure 1), recovering thin layers of tephra interbedded with siltstones . Based on this evidence, we interpret the cone apron to be comprised of fine-grained layers of tephratransported by subaqueous eruption plumes, likely interbedded with reworked material from cone collapses and degradation, a phenomena commonly observed in volcanoes elsewhere [25, 102, 124]. The cone apron may also contain minor subaqueous lavas that overspill from the crater rim, and possible peperitic material associated with invasive lavas and/or shallow type-4 intrusions . The 3D seismic interpretation of a submarine monogenetic field along the southern Australian margin shows that submarine lava-flows could extend for more than 30 km from the eruptive centre .
The tephra fallout carpet of cone-type volcanoes (like their counterpart crater-type volcanoes) is seismically unresolved and thus must be based on studies elsewhere [99, 109, 111]. Submarine eruption plumes (and also sub-aerial pyroclastic density currents entering the water) can introduce pyroclasts and rock fragments into the water column, while residual buoyant material remains suspended and can be transported by oceanic currents [106, 107, 110, 123]. Rafts of highly vesiculated pumice can travel long distances when carried by currents [125, 126]. When saturated in water, these fragments sink and can form deposits with size varying from ash to blocks . These processes are possible to have occurred in the MVS.
MVS cone-type volcanoes contain syn-eruptive architectural elements that show reflectors piling-up above the PrErS horizon. The vent structure of these volcanoes shows minor excavation into the PrErS horizon, which suggests that the effects of eruptions on the host rocks are minimal, when compared to those of crater-type volcanoes . The flanks of cone-type volcanoes typically are outward-dipping from the central crater and display low-to moderate-amplitude, which suggests that they more likely comprise fragmented material ejected during pyroclastic eruptions rather than formed by lavas.
The tephra flank and cone apron of cone-type volcanoes predominantly have low slope angles (<16∘), typically displaying widespread seismically detected boundaries up to 6 km from the central crater. This geometric characteristic together with information from rock textures recovered in Resolution-1 (possible armoured lapilli and ash aggregates) suggests that this volcano-type represents a deep-water equivalent of tuff cones [35, 38]. However, we do not reject the possibility that spatter cones and pillow mounds also occur in the MVS, which could be verified by acquiring additional high quality 3D seismic data and/or drilling holes proximal to their eruptive vents.
Sedimentological and volcanological processes observed on modern volcanoes [11, 25, 26, 67, 124], suggest that the syn-eruptive interval of the MVS may comprise sedimentary deposits triggered by simultaneous eruptions, together with primary volcanic eruptive deposits. Processes related to the eruptions such as earthquake shockwaves, submarine explosions, and magmatic inflation are potential triggers for debris flows, submarine landslides and cone-sector collapses (e.g. submarine landslides triggered by the 2009 eruption at NW Rota-1 volcano, Mariana arc; . Tephra material can be reworked during or immediately after eruptions by mechanisms such as submarine currents, waves and tsunamis [25, 128]. Based on the available 2D seismic data and a limited number of wells, distinguishing eruptive volcanic deposits from eruption-related sedimentary deposits, or from resedimented epiclastic deposits is not always possible. We tentatively infer five settings in which distinctive sets of eruption-related sedimentary architectural elements can form (Figures 6, 16 and 19), based on seismic facies that could indicate reworking of parts of the volcanic edifices during the syn-magmatic stage (e.g. chaotic seismic facies, sediment waves). These five settings are: (1 and 2) the crater zone of both volcano types; (3) the flanks of cone-type volcanoes; (4) the tephra ring of crater-type volcanoes; (5) the cone apron of conetype volcanoes.
The crater zone of MVS volcanoes may contain sedimentary deposits controlled by gravitational flows and other types of mass transport deposits that infill the space created by explosions and ground collapses during (and immediately after) eruptions. Common sedimentary facies in the crater zone may include course-grained, massive, chaotic and amalgamated deposits formed by tephra re-working followed by slip and deposition into the crater (Figure 17), and by slide and slump blocks collapsed from the crater walls[25, 28, 114]. On the flanks of cone-type and along the tephra ring of crater-type volcanoes, material reworking by currents and mass-wasting are important syn-and post-eruptive process ([101, 106, 124, 129]. On the cone apron of pc-14 (Figure 19), seismic images show a characteristic facies that resembles sediment waves occurring between the PrErS and PoErS horizons, which may represent syn-eruptive submarine landslides such as those reported by .
Monogenetic volcanic fields are typically characterised by a cluster of dispersed and isolated volcanoes formed by one eruptive cycle with minor interruptions [13, 24, 25, 88, 100]. Individual volcanoes are typically diachronous with one another, each having an active life of years to centuries , and the complete volcanic field taking hundreds of thousands to a few million years to form [130, 131, 132, 133, 134]. Therefore, despite the fact that monogenetic volcanoes are defined by short eruptive periods, the magmatic system itself may have been long lived .
In our volcano-stratigraphic model (Figure 4 and 6), inter-eruptive architectural elements can be formed in association with volcanoes that have finished their eruptive cycle, but may have begun to degrade and interact with basin sedimentation while volcanism is still active in other parts of the MVS. In polygenetic volcanoes, syn-and intereruptive deposits are commonly interbedded near a relatively stationary eruptive centre. By contrast, in monogenetic volcanic fields, these inter-eruptive sedimentary deposits typically are interbedded with primary volcanic deposits erupted from diverse and scattered vents. In the MVS, inter-eruptive architectural elements are represented by sedimentary rocks of the Tokama Siltstone interbedded with volcaniclastic rocks that likely were erupted from different MVS vents. In addition, inter-eruptive deposits related to mass transport and erosion of inactive volcanoes are likely to occur in the MVS, although, we cannot separate these rock units from syn-eruptive sedimentary deposits, due to limitations in the resolution of the seismic dataset.
Sedimentary processes, such as erosion and burial of the volcanic edifice, are dominant during the post-magmatic sequence (Figure 4 and 6). After the magmatic activity in the MVS had ceased at ca 11.5 Ma , the submarine volcanic morphology had a strong impact on the sedimentation patterns of the study area. We divide the post-magmatic sequence into degradational and burial stages. Each stage is marked by different processes of erosion and burial of the volcanic edifices, which control the formation and distribution of MVS post-magmatic architectural elements.
The degradational stage is marked by high rates of erosion of the MVS edifices. We place the PoDgS coincident with a late Miocene (lM) unconformity, because this erosive surface represents the last significant event that degraded the volcanic edifices  (Figure 6). Architectural elements of this stage comprise canyons, gullies, localised epiclastic deposits and contemporaneous non-volcanogenic sedimentary deposits impacted by the presence of the volcanoes (Figures 13, 16, 19 and 20).
Canyons and gullies are usually associated with the PoDgS and vary in size from <100 m to 1100 m wide and up to ca 175 m deep, considering the acoustic velocity of 2500 m/s for the Tokama Siltstone recorded in sonic wire-logs of Resolution-1. Channels are narrow towards shallow water and wider and more deeply incised at the slope/abyssal interface. Occasionally these channels are stacked at the base of the tephra flank and cone apron of cone-type volcanoes (Figure 19). Canyon erosion can remove material from the volcano flanks, which may cause instability and collapse of parts of the cone, forming localised small debris deposits (Figure 6). However, if these debris deposits occur in the MVS they are seismically unresolved with the available dataset.
Volcanoes with flattened tops concordant with the PoDgS typically show reflectors downlapping from the edifice onto the basin floor, suggesting that these volcanoes provide a local source of epiclastic sediments (Figure 6 and 20). Seismic attribute analysis shows that these deposits likely contain material eroded from the volcanoes, due to their similarity in seismic impedance analysed from diverse seismic attributes (Figure 20). This degradational seismic facies only occur in association with reconstructed volcanoes > 200 m high located proximal to the 11 Ma shelf-break . We interpret this degradation facies to represent a plume of epiclastic sediments eroded from volcanoes that were emergent and/or eroded in a shallow marine environment by the action of waves and shallow currents.
The epiclastic plume is deposited parallel with the direction of the prograding clinoforms, with maximum seismically detected horizontal and vertical dimensions of up to 3 km and 70 m, respectively. The epiclastic plume probably represents sediments deposited next to extinct volcanic islands that had emerged above sea-level by the late Miocene (Figure 20). Similar seismic facies are evident in the Vulcan-3D seismic dataset, located in the offshore Taranaki Basin (Bischoff, unpublished data).
Among cone-type volcanoes, we observed a characteristic seismic facies comprising horizontal and parallel continuous reflectors, here referred to as inter-cone plains (Figure 6, 21 and 22). The seismic facies of the inter-cone plains are similar (moderate-amplitude, semi-continuous and parallel reflectors) to those intersected by the Resolution-1 where fine-grained sedimentary rocks of the Tokama Siltstone were recovered. This seismic character suggests that the inter-cone plains were mostly confined to volcanic edifices, and formed by non-volcanogenic sedimentary strata deposited by processes of decantation in a low-energy environment. However, minor epiclastic deposits may occur next to the flanks of the volcanoes, interbedded with sediments of the inter-cone plains. Figure 23 shows the paleogeography of the study area at the time of the formation of the PoErS horizon, and the location of the shelf-break position at 11 Ma (PoDgS).
In seismic images, the burial stage of the MVS is characterised by stratal geometries showing evidence that the volcanic edifies impacted local sedimentation for millions of years after they were buried. This stage is marked by high rates of burial and little or no degradation of the volcanic edifices that remained unburied after the late Miocene unconformity (i.e. PoDgS). Seismic reflectors above eleven cone-type volcanoes display a domal structure, here referred to as burial dome, suggesting the presence of a persistent bathymetric high after these volcanoes were buried (Figure 19). The processes that resulted in the production of the burial dome likely include differential compaction between the volcanic and enclosing sedimentary strata [6, 81, 135].
Because the impact of buried volcanoes in the basin architecture varies from one volcano to another, we place the PoBuS according to observations from domes located above the volcano pc14, which show impacts in the geometry of overlying strata until at least the Opoitian NZ stage (ca 5 Ma; Figure 19). Canyon scars located on the edges of the burial dome above pc14 provide evidence that the location of this buried edifice impacted basin sedimentation until at least ca 6 Myr after volcanism in the MVS has ceased, and ca 1 Myr after pc14 was completely buried. Seismic images of these peripheral canyons (i.e. around the margins of the burial domes) are likely to be associated with the deposition of submarine fans up to 2kmwide (Figure 19). Fans such as these are well imaged from 3D seismic data over the buried Kora Volcano, in the offshore Taranaki Basin, referred to as seamount-edge fans by .
The processes that control the deposition of these fans remains poorly investigated, but are likely to involve either erosion around the burial dome, due to local formation of a hard seafloor substrate associated with the dome structure, or could be related to carbonate deposits at the top of the domes.
Reconstruction of the architecture of the Maahunui Volcanic System(MVS) enables us to understand how igneous and sedimentary bodies interact and are distributed in space and time within the northern part of Canterbury Basin. MVS comprises 25 main intrusive, extrusive and sedimentary architectural elements that are systematically distribute into three first order magmatic sequences (i.e. pre-, syn-, and post magmatic). The architecture of the MVS resulted from four second order magmatic stages associated with (i) emplacement of magma at the sub-volcanic level, (ii) construction of a volcanic sub-sea morphology, (iii) degradation, and (iv) burial of a monogenetic volcanic field in a sedimentary basin. The MVS plumbing system comprises mainly saucer-shaped sills, sill and dike swarms and minor laccoliths, divided systematically into five plumbing-types. The geometries and sizes of these intrusive architectural elements are determined by their level of emplacement, and by their spatial relationship to host sedimentary strata. The extrusive part of the volcanic field was erupted entirely in a deep marine setting (ca 1000 m water depth), and contains at least 31 deep-water equivalents to crater-type (i.e. maar-diatreme volcanoes), and cone-type volcanoes (i.e. tuff cones). Crater-type volcanoes have eight main syn-eruptive architectural elements: root zone, lower and upper diatreme, tephra ring and tephra plain, intra-crater cones, overspill wedge and tephra fallout carpet. Cone-type volcanoes have five main syn-eruptive architectural elements: basal cone, central crater, tephra flank, cone apron and tephra fallout carpet. Each of these syn-eruptive elements formed by a combination of eruptive and associated sedimentary deposits, with minor and localised intrusions. After volcanism ceased, degradation and burial of the volcanic edifices strongly affected local sedimentation for at least ca 6 Myr after the volcanoes ceased erupting, and ca 1 Myr after they were completely buried. Degradation and burial of the volcanic edifices of the MVS produced five main sedimentary architectural elements (i.e. inter-cone plains, epiclastic plumes, canyons and gullies, burial domes and seamount-edge fans). This study demonstrate the value of detailed seismic stratigraphic analysis coupled with information from borehole data, and analogy with volcanological processes that occur elsewhere. Understanding the time and space relationships between the diverse architectural elements permits us to reconstruct the complete architecture of the MVS, including its shallow (<3 km) plumbing system, morphology of volcanoes, and their impact on the host sedimentary basin during their degradation and burial. Insights from the architecture of the MVS can be used for exploration of geoenergy resources such as oil, gas and geothermal energy in buried and active mono-genetic volcanic systems elsewhere.
We would like to thank IHS Markit and Schlumberger for providing academic licence to use the Kingdom and Petrel software. We are grateful to the New Zealand Petroleum and Minerals and the Ministry of Business, Innovation and Employment of New Zealand for providing the dataset and funding for this study. Thanks for the constructive reviews of Károly Németh and an anonymous reviewer.
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