Basaltic eruptions have been observed to produce structurally complex, compound 'a'ā lava flow fields but their morphometry has only rarely been systematically documented. We document the morphology and structures that developed during the emplacement of the 1982 basaltic lava flow field at Mount Cameroon (MC) volcano over a period of one month. Topographic cross-sections (13 in total) were made from the main vent (~2700 m above sea level (a.s.l)) down to a distance of 5.5 km on the cooled lava surface. Details obtained from these cross-sections include: channel width and depth, levee slope, lava surface morphology and structures. These details enabled us to describe the physical characteristics of the 1982 lava flow field. The inclined (12° - 19°) underlying slopes on which this flow field was emplaced resulted in a characteristic channelized basaltic 'a'ā flow field morphology. This includes a proximal zone characterised by reduced flow width and depth with no subsidiary channels. Slab-crusted lava dominates the proximal channel distinctively bent into convex upward shapes. 7 secondary vents were observed for the first time ~2.5 km from the main vent, with heights of 3 - 15 m. This is a very significant observation since it points to the fact that the flow field emplacement may have been a product of 2 eruption sites as observed at other historical MC lava flow fields. This supposition was ruled out by further evidence obtained from other surface features within the flow field. The presence of these secondary vents still has an important bearing in lava flow hazard assessment. Field observations also revealed the presence of tumulus. This is a novel feature for MC lava flow fields. It displayed a close similarity to those observed at other basaltic volcanoes occurring in association with clinker 'a'ā lava, lava tubes, squeeze-ups and pressure ridges. Channels are well-defined, bounded by levees. Accretional and overflow levees dominate in this flow field. This lava flow-field attained a final length of 7.5 km, an area of 2.6 × 106 m2 and volume of 1.3 × 107 m3. The presence of tumulus indicates internal inflation together with structures such as pressure ridges and squeeze-ups which are also attributed to compressive forces. Our observations suggest that real-time monitoring of compound lava flow fields evolution at MC may reveal the emplacement mechanisms of complex structures such as the secondary vents (~2180 - 2011 m a.s.l.) observed within the flow field. In addition, documenting the occurrence, morphology and link between lava tubes, tumulus and squeeze-ups may allow us to determine the risk of reactivation of a stalled flow front. This will thereby enhance the ability to track and assess hazards posed by lava flow emplacement from MC-like volcanoes.
The advance of lava flows produced by volcanic eruptions has been studied through field observations [1-12]; remote sensing techniques [13-17], as well as through analytical or numerical modelling [18-23]. The above cited methods have greatly improved understanding of the emplacement dynamics of lava flows as they provide clues about key processes occurring during eruptions even for flows not witnessed. However, the physical volcanology of most lava flow fields in developing countries has received limited systematic attention.
Lava morphological data are significant to understand lava emplacement mechanism and anticipate impacts from effusive eruptions. Lava flows can cover long distances in 3 - 6 days, damaging properties and threatening lives [2,24,25]. The complex morphologies characteristic of long duration basaltic 'a'ā lava flow fields reflect the importance of processes such as inflation, formation of lava tubes and secondary vents [17]. The identification of secondary vent sites of lava flow fields is critical for lava flow hazard assessment [17]. They have been observed to allow flows to lengthen significantly over their forecasted cooling-limited lengths [26]. In contrast, overflow events or new lobes development favour flow field widening [27] instead of flow lengthening.
Advances in lava flow modelling in the past 25 years show that it is increasingly possible to anticipate the final lengths and spatial spread of single flow units [18,28]. However, during basaltic eruptions, complexities like new flow units are emplaced alongside and on top of earlier units resulting in compound flow fields [5,6]; channels crust over and lava tubes, secondary vents, squeeze-ups and tumulus develop. The development of these features hinders accurate modelling of long-lived (>1 week) basaltic 'a'ā lava flow fields [17] which is not accounted for in these models. To improve understanding on the development of compound lava flow fields and the dynamics of any volcanic system, it is recommended to quantify lava morpho-structures in detail both during and after emplacement [6,29].
Studies of terrestrial lavas suggest that the overall development of flow fields is systematic and that a general, normalized relationship can be established linking the final dimensions of a flow field to underlying slope, eruption duration, discharge rate, gravitational acceleration, lava density and rheology [27,30,31]. Linking qualitative and quantitative measurements of lava flow surface morphology with historical observations of eruptions is an important, but yet underexploited route, to constrain emplacement mechanism of basaltic lavas.
Basaltic lava flow fields often demonstrate compound morphology. That is they are comprised of several flow units and lobes with some superposed on each other [5, 17,32]). A flow lobe here refers to an individual package of lava surrounded by a chilled crust [1]. Compound here refers to a lava flow field made up of two or more flow lobes of any geometry or size [1,33]. The development of compound basaltic 'a'ā lava flow fields is a common phenomena at Mount Cameroon (MC) volcano as exemplified in the 1959, 1982, and 1999 lava flow fields [2,8,34]. Most published data existing at MC (Figure 1) are limited to its seismicity, eruption dynamics, petrology and geochemistry of specific eruptions that occurred in the 20th and 21st centuries [2,24,25,34-40]. Recently, a few studies started focusing on lava flow morphology [2,8,11] and hazards [35,41-43] at MC.
Eruptions that produced basaltic lava flow fields from MC have been associated with significant impacts over the past years. The 1922, 1959 and 1999 eruptions posed major threats to agro-allied complexes and road infrastructure around the SW [24,25] and NE [2] flanks (Figure 1). Common phenomena observed for most historical eruptions at MC are that they are all fissure eruptions with venting typically at more than one site (1922, 1959, 1999, 2000; Figure 2; [2,8,11,24,25,40]). Upper sites are dominated by more explosive activity building large pyroclastic cones, whereas lower sites emit the largest volume of lava. The principal lava type produced ranges from pahoehoe (ultra-proximal) to 'a'ā (dominant flow morphology) and blocky lava observed at the distal end [11]. Petrographically, all these lavas are porphyritic [2,25,39] with the exception of the 1982 lava that is nearly aphyric [2,25,34].
In October 1982, an eruption that produced seismic swarms widely felt around Buea (SE flank; Figure 2), occurred on the SW flank of MC. The physical characteristics, composition and evolution of the 1982 lava flow field have been described by [34]. Other aspects including its petrology and geochemistry have been analysed by [2,25,39]. So far, no systematic field survey has been carried out on the 1982 flow field to document its morphology or quantify down channel geometry. Here, a systematic field study was carried out on the 1982 flow field with the primary objective of obtaining geometric parameters (width and depth) of the stable channel zone that fed the flow from source to the distal transitional-dispersed flow zone.
The goal of this paper is to describe the morphology and structures observed within the stable and transitional channel zones of the 1982 lava flow field as defined by [44]. Based on their observations of basaltic 'a'ā flow fields at Mauna Loa, Hawaii, [44] divided lava flow fields into four zones from vent to toe: 1) stable channel; 2) transitional channel; 3) dispersed flow zone and 4) flow toe. We present observations and field measurements made after the emplacement of this lava flow field, covering the proximal part fed principally from the source scoria cone (emplaced on characteristic slopes of 14˚ - 18˚) and the transitional zone (12˚ - 19˚).
The 1982-lava flow field offers an excellent opportunity to examine the large-scale structural evolution of a compound flow field as well as the complex surface features that are ubiquitous in most 'a'ā flows. Such intermediate-long lived eruptions emplaced on inclined slopes offer good opportunities to investigate the effect of slope on 'a'ā lava flow fields in terms of surface morphology and inferred emplacement. So far few studies have described long-lived basaltic lava flow field morphologies and emplacement processes on inclined [11,31] and extremely steep slopes [45]. Numerous studies however exist on the morphology of long-lived basaltic lava flow fields emplaced on flat to gently sloping surfaces [27], [46]. From this analysis, we document in detail the latestage development of this flow field which includes the formation of the secondary vents (short-lived ephemeral vents), lava tubes and tumulus and consider implications for lava flow hazard assessment. We also consider the role of effusion rate fluctuations for channel geometry fluctuation. Field measurements were used to constrain flow rheology. Such constraints are essential for a follow-up effort where lava flow hazard will be quantified.
2. The Geology of Mount Cameroon and the 1982 Eruption Chronology2.1. Geological Context of Mount Cameroon (MC)
MC is the largest and most active of the continental volcanoes of the Cameroon Volcanic Line (CVL; Figure 1). The CVL is a major tectonic feature in West-Central Africa that runs SW-NE following a major left-lateral fault system that extends for more than 2000 km, from Pagalu Island into West-Central Africa (Figure 1). The origin, geology, structure and petrology of the CVL have been discussed by several authors: [35,47-51]. The CVL’s origin is still subjected to debate. The most widely accepted structural explanation for the origin of the CVL is that it is a product of Cretaceous reactivation of PanAfrican strike-slip faults trending N70E [38,48,52].
MC is a steep volcanic shield covered by successions of lava flows [11,53] and subsidiary scoriae deposits (Figure 2). It has a flat summit plateau, a rift zone defined by a linear cluster of eruptive vents, a deep valley (elephant valley) in the N flank, topographic steps at the base [53] together with numerous faults and fissures mostly trending N40E [35]. It is composed entirely of moderately alkaline basic lavas (alkaline basalts, hawaiites, picrites and mugearites [35,48,49]. Field observations indicate that lava flows are massive, porphyritic or vesicular. Moderately explosive Strombolian activity is common at high elevation vents [11,24,25], but lava flows are the most common products released from MC eruptions. Over historical times, most lava flow activity has
been confined to the summit, SW and NE flanks of MC (Figure 2). This has effectively protected the SE and NW flanks from lava inundation.
Historical lava flows have flow lengths from ~850 m (upper 2000) to 11.5 km (1922, lower 1999; Figure 2; [11,41]). They cover an estimated surface area of 26.5 km2 in the last 110 years at MC (Figure 2). Observations of effusive events at the MC summit are extremely minor, characterised by flows with limited extents that stay within the confines of the crater (e.g. 2000 site 1 flow; Figure 2). In addition, vent types differ between minor and major effusive events. Minor effusive events are fed by persistently active strombolian vents within the crater that host lava lakes which release the lava by breaching of the cones. In contrast, most vents on MC that feed major effusive events result from secondary vents/ephemeral boccas breaching or tapping from the central magma column somewhere below the level of the summit vents [11].
The next most abundant products observed at MC are pyroclastic cones (~340 cones have been mapped) aligned along a NE-SW trend (Figure 2), corresponding to the CVL alignment (Figure 1). They have the highest spatial density on the upper SW flank of MC (Figure 2). These cones result mostly from the observed moderately explosive activity and range from small spatter mounds to larger spatter-scoria cones. Other observed formations include lahars (volcanic mudflows; Figure 2) graded as a possible ancient hazard around MC [42]. Etindites (nephelinite lavas) are restricted to Mount Etinde (small volcano probably of Miocene age on the lower SW flank of MC; Figure 1; [35,54]). Lastly, are underlying sediments upon which all the above rock types lie (Figure 2; [35]).
2.2. Evolution of the 1982 Lava Flow Field
On 16 October 1982, new effusive activity started at MC and continued until 23 November 1982. This eruption occurred after 23 years of quiescence and emplaced a ~7.5 km-long basaltic 'a'ā lava flow field (Figure 3). A detailed account of the chronology/sequence of this eruption has been given by [47]. Thus, we summarise only elements of the chronology pertinent to the analysis of the lava flow field evolution presented here. Lava, ash, gases and tephra were emitted from a SW-NE trending fissure at an elevation of ~2700 m above sea level (a.s.l.) on the SW
flank of MC. The observed fissure extended over a distance of ~1 km down slope.
Moderately explosive activity at the upper end of the fissure led to the formation of a 25 m high scoria cone by November 7 (Figures 3(a) and (b)). A lava channel with an initial width of 3 m was observed in the first few days of eruption (Figure 3(c)). Lava flowed in this channel at a velocity of 5.2 m∙s−1 and initial magma discharge rate of 10 - 30 m3∙s−1 which dropped to ~0.1 m3∙s−1 in the last 24 hours of eruption. Approximately 900 m down slope from the cone (8 November), measurements of an active lava lobe showed that it was 3.5 m wide, 1.25 m thick and advanced with a mean velocity of 0.2 m∙s−1 on a slope of 18˚. Temperature readings at this point in the flow using a thermocouple produced values of 1045˚C ± 5˚C - 1070˚C ± 5˚C. This led to estimation of initial eruption temperature at 1160˚C and to average cooling rates of 0.1˚C - 0.3˚C∙s−1. This lava lobe entered dense forest at 2400 m a.s.l., 1.5 km from the cone. Flow front measurements from the main flow lobe (Figure 3) at 1000 m a.s.l. gave values of ~200 m wide and 20 m high.
Between 30 October and 4 November, a landslide occurred just below the main cone (Figure 3(d)) that initiated a debris flow composed of a mixture of older volcanic material and the only just emplaced 1982 lava flow. This debris flow modified the upper part of the 1982 lava (Figure 3(d)) acting as a blockage zone and stopped 1.5 km from the vent. It produced an elongated depression with a length, width and depth of 500 m, 200 m and 150 m respectively. [47] estimated the total lava volume extruded at ~107 m3. Other estimated parameters for this eruption include maximum pre-eruptive water content for the magma at 0.6 wt%, viscosity (104 Pa∙s), yield strength (104 Pa) as well as petrographic and geochemical data.
The emplacement of this lava flow field on moderately inclined slopes (12˚ - 19˚) resulted in distinctive flow field morphologies. The development of a compound lava flow field characterised by several lobes (Figure 3), present an excellent opportunity to examine the morphology and evolution of an intermediate/long-lived 'a'ā lava flow field emplaced on inclined surfaces. Unfortunately, during the 1982 eruption, virtually no information (e.g. GPS and ground control points for observed features), was collected from which the flow field morphology and evolution could be examined. Here, fieldwork was carried out to map out observed features and structures on this flow field and describe the surface characteristics of the flow. This data was then used to present details of the morphology and evolution of the flow field, and relate this evolution to quantitative parameters such as slope, effusion rate, number of active vents, flow length, lava tubes and number of active flow lobes. In doing this, we define the characteristics of the 1982 basaltic lava flow field inferred from its emplacement dynamics. From field observations and the narrative given by [47], the lava flow was extremely unstable and suffered from almost constant flow front collapses to feed other flows extending down-slope from stalled flow fronts.
3. Materials and Methods
Field observations and measurements (channel width, depth and levee angle) were made at the proximal, medial and dispersed flow portions of the flow field. Details of the surface morphology for the different lava types and structures observed in this flow field were obtained across transversal profiles made within the stable and transitional flow zones. 13 profiles (Figure 4) were measured using a 30 m tape, an abney level and a compass clinometer. They enabled to describe the physical characteristics of the 1982 lava flow field. Four representative profiles are illustrated here to show changes in channel morphology down-flow (Figures 4(a)-(d)).
Morphology of the flow field at a distance (length) above 5.5 km (that comprised the dispersed and flow front zones) could not be observed because this portion of the flow is buried by the lower 1999 vents and lava (Figures 1 and 2). Several bifurcations, islands and flow lobes are observed. Our focus is on the WSW branch of the flow field (Figure 3).
Lava thickness was derived from trigonometry. These values were substituted in equations from [55,56] and into Jeffrey’s equation to estimate yield strength (levees)
and mean channel velocity (Equations (1) and (2)).
where t is yield strength, r is the dense rock equivalent density, g is acceleration due to gravity which is equal to 9.8 m∙s−2, t is levee thickness and a is the gradient of slope (slope here represents pre-eruptive down flow slope).
where V is mean velocity, a is the pre-eruptive down flow slope (obtained from the field and the 30 m Digital Elevation Model (DEM) for MC) and B is the shape constant considered to be equal to 3 (value is representative of wide channels).
From the estimated velocity (V), channel depth (d) and width (W), effusion rate for lava flowing in these channels was derived (see [57]). A uniform density of 2700 kg∙m−3 was assumed in estimating the above rheological parameters. This is an average density for this lava flow estimated based on previously published whole-rock geochemical compositional data from [25,39,47]) following [58] approach. Lava volume for this eruption was reestimated by the planimetric approach proposed by [59]. This involves the measurement of the area covered by the lava flow field (obtained from GIS estimate) multiplied by an estimated mean lava thickness for the flow field.
For the purpose of reconstructing the stable channel geometry, profiles were made at intervals of 100/200 m (for the first one kilometre) and at 1 km interval from then onwards (Table 1) starting with a profile within a few metres from the vent (Figure 4(a)). Other observations from this flow were obtained between profiles.
4. Results4.1. Lava Flow Field Morphology
The 1982 compound 'a'ā lava flow field (Figures 4(a)-(d)) has 6 main and uncountable subsidiary lava flow lobes which branch out in several directions, with some of them meeting up again towards the flow front (Figure 3). The principal flow morphology observed from near-vent to 5.5 km distance for this lava flow field is clinker 'a'ā lava followed closely by blocky 'a'ā lava. Upper flow proximal lava in the first 17 m from the vent is slabcrusted lava within the stable channel according to the terminology given by [60]. Most morphological features indicative of lava flow emplacement mechanism and late stage deformation were recorded.
4.1.1. Large-Scale Flow Field Development and Structures
1) Scoria Cone The development of the main cone thought to have fed the greatest volume of the lava flow field was partially documented by [47]. This cone is visible both on Landsat TM, ETM+ scenes, and in the field (Figure 5(a)) emplaced on slopes of 16˚ - 18˚ and breached in the downflow direction. Measurements (GIS) made from the already emplaced 25 m high cone gave ~350 m base diameter and ~85 m crater diameter, occupying an area of ~1.2 × 105 m2 and volume of ~2.5 × 106 m3 (~20 m thick) respectively. Lava-fountaining up to 300 - 400 m high from this cone ([47]; Figure 3(a)) in its explosive phase, led to emplacement of a tephra layer observed for a distance of up to ~200 m away in the NE direction (along the route used to get to the vent). This layer was sparsely dotted by large bombs (~1 m) made up mostly of lapilli and sand-sized particles close to vent that became finer away from it (Figure 5(a)). The scoria and lapilli range in size from 2 to 65 mm in diameter.
The blockage (Figure 5(a)) observed immediately after the cone breached zone was produced ~14 days after eruption onset [47]. It resulted from a landslide below the cone that produced a debris flow of old volcanic material (ash and scoria) mixed with disrupted remains of the 1982 lava [47]. This blockage came after the establishment of the stable channel (Figure 5(a)) observed immediately after this zone [47]. The observed blockage at the time of eruption prevented the debris flow from taking the direction of the channel. The debris flow deposit was still preserved in the field at the time of the study in the upper sector of the flow field (Figure 5(a)). This debris flow ended with a sharply defined lobate front as described by [47]. It obstructed the flow of lava in the established channel (Figure 5(a)) causing diversion of the flow that led to the production of a secondary channel to the West of the vent which merged a few metres downflow with the primary vent.
2) Secondary Vents Field investigations revealed a series of 7 late-forming secondary and/or ephemeral (short-lived) vents (Figures 5(b) and (c)). These vents are observed ~2.5 km away from the main vent (Figures 5(b) and (c)) at ~2180 m a.s.l, emplaced on slopes of 15˚ - 19˚, all aligned in the E-W direction within the flow field. These small vent constructs are 3 to 15 m high (Figure 5(b)), are most often breached in the SE direction (Figure 5(c)), and are spaced at intervals of 2 to 10 m of each other. Threequarters of them produced lava with clinker 'a'ā morphology that flowed in distinct channels within the flow field which disappeared ~20 m down flow. Most of their walls have already been colonised by mosses. Close inspection revealed that some of these walls are plastered with spatter and clinker (Figures 5(c) and (d)).
3) Levees Few initial levees were preserved because of variations in flow level and blockages within channels that fa-
Geometrical parameters of the stable channel zone of the 1982 lava flow field
voured over flow events and formation of overflow levees. These events modify levees (Figure 6(a)) and cause flow field widening. Initial levees are characterised by outer slopes of 26˚ to 66˚. These levees are 0.3 to 2 m thick (t) with corresponding levee widths of 0.4 to 3 m (Figures 4(a)-(d), Profiles 1 - 4). Yield strength of initial lava estimated using outer initial levee thickness and angle of rest [55] fluctuates between 103 to 104 Pa across the different profiles. The main lava types that characterised these levees are loose clinker and blocky 'a'ā lava
(Figures 4(a)-(d), Profiles 1 - 4). The inner walls of these levees show horizontal layering and shearing features (Figure 6(b)).
Overflow levees could be distinguished from initial levees because they showed layering of different lava levels believed to represent different flow episodes. Overflow material is basically clinker and blocky 'a'ā lava (Figure 6(a)) and to a limited extent rubble 'a'ā lava (Figure 4(c), profile 3). Typical outer slopes for overflow levees are 30˚ to 50˚ with levee thickness (t) values of 0.4 to 2.5 m and levee widths of 0.3 to 2.6 m.
Accretionary levees (Figures 6(b)-(e)) are the dominant levee type. Accreted/agglutinated lava surfaces were observed both on the outer and inner walls of channels. They are characterised by brecciated surfaces (Figure 6(c)) showing shearing features, tension fractures and cooling cracks (Figure 6(d)). They are 0.5 to 8 m thick. Virtually all of the internal accretionary levees observed are characterised by sub-vertical to vertical inner levee walls (Figures 4(a)-(d), Profiles 1 - 4) with a massive interior texture (Figure 6(e)). Yield strength estimated for this levee type is stable at 104 Pa. Since the flow front could not be observed at the time of this study, no flow front measurements were made. However, [47] gave a width of ~200 m with a thickness of 20 m for the main flow lobe.
4) Lava Channels In this flow field, as for other 'a'ā dominated lava flow fields at MC (e.g. 1959, 1999) channels were the dominant preserved transport pathway. Lava in proximal channels (first 100 m) flowed with initial estimated velocity and effusion rate of 4 m∙s−1 and 3.3 m3∙s−1 respectively. Channels are 0.85 - 5 m wide, dominated by slab-crusted lava with clinker 'a'ā margins (Figure 5(a); Table 1) observed up to a distance of 205 m (Figure 7(a)) away from vent. However, these crusted surfaces are not continuous for the whole length of the 205 m. They broke up into slabs after covering distances of 10 to 17 m (Figure 7(b)). These distances correspond to an increase in slope from 16˚ (at-vent) to 18˚ (300 m). These broken slabs probably acted as temporary blockage zones within these channels (Figure 7(c)) while this flow was active. Broken slab material usually piles up forming heaps up to 13 m long at some locations (Figure 7(c)).
Within a few metres (~20 m) from vent, secondary channels were observed at the sides of the primary or main channel (Figure 7(c)). These channels are 2 to 3 m wide, 100 m from vent Figure 7(c)), and 30 m wide ~400 m from vent (Table 1). Effusion rate increased to ~29 m3∙s−1 (100 m distance) and dropped to 13 m3∙s−1 200 m away from vent. This drop in effusion rate led to the production of channels (~200 m from vent) characterised by a reduced width (1.5 m) and an increased depth (5.4 m) with a slab-crusted surface that continued for a distance of 10 m before breaking up into slabs (Figures 7(a) and (d)). Velocity estimates at these distances had dropped to 2 and 1.4 m∙s−1. Both effusion rate and velocity (12 m∙s−1) increased from these distances up to 1 km distance. This favoured the formation of wider channels (6 - 21 m) and clinker and blocky 'a'ā lava emplaced on slopes of 14˚ - 17˚. The widest channel (113.5 m) in this flow field was observed ~2 km from vent
hosting sealed lava tube surfaces, characterised by reduced velocity (4.5 m∙s−1) and high flow rates (68 m3∙s−1). Channel material is clinker 'a'ā emplaced on a slope of 15˚.
Lava channels were still considerable wide (10 - 22 m) from this distance but dropped to 6 m, 5.5 km from vent. At this distance, velocity and flow rate had dropped to 0.3 m∙s−1 and 13 m3∙s−1 respectively. The lava type here is clinker and blocky 'a'ā lava emplaced on slopes of 12˚ - 14˚. From the estimates made, an average velocity and flow rate of 4.5 m∙s−1 and 26 m3∙s−1 were produced for this flow. Taking an average lava thickness of 5 m (±2 m; field estimates), an area of 2.6 × 106 m2 (GIS estimate), this eruption produced lava with a volume of ~1.3 × 107 m3.
5) Lava Tubes Lava tubes were first observed in channels at a distance 600 m from vent (Figure 7(b)). They could be distinguished based on their elongated forms, continuous surface morphology, raised margins and extensive lengths relative to that of the surrounding rocks (Figures 7(b) and (c)). These tubes are characterised by a spinose surface with crusts just a few cm thick (Figure 7(b)). At 600 m distance, an observed lava tube is 10 m long and ~2 m wide (Figure 7(b)). These lava tubes were abundant within the primary channel (~2 km from vent) where the channel is widest. From their surface appearance, 5 could be distinguished with extensive lengths (~10 - 20 m) that became buried down-slope by channel material. This is 500 m (up-slope) from the point where
secondary vents were observed.
4.2. Down-Flow Channel Geometry and Small Scale-Structures
Here, on the basis of channel geometry fluctuation, we split the stable channel zone of the flow into three sections: 1) an upper section characterised by wider than deep channels; 2) an intermediate section governed by deeper than wide channels and 3) a lower section where channels resume their normal trend as in the upper section being wider than deep. This zone is followed by the transitional channel zone observed ~4 km down-flow.
4.2.1. Stable Channel Zone
Table 1 and Figures 8(a) and (b) give details on the stable channel geometry at a distance starting from 1 m from the vent, progressively down-stream. The widths of breakaway/side channels are also given at the corresponding
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