Spatial structures of hydrothermal vents and vent-associated megafauna in the back-arc basin system of the Okinawa Trough, western Pacific
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- Tokeshi, M. J Oceanogr (2011) 67: 651. doi:10.1007/s10872-011-0065-9
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Spatial patterns and morphology of hydrothermal vents and the occurrence of vent-associated megafauna were investigated in the back-arc basin system of the Okinawa Trough, western Pacific. Amongst hydrothermal vent fields located on the rising slopes to the NE and S of the basin, the Iheya North area has been subjected to a series of intensive diving surveys. Hydrothermal vents demonstrated concentrated patterns of distribution on different spatial scales. In Iheya North, the majority of vents occurred in lines parallel to the NE to W/SW alignment of the spreading axis, within a radius of ca. 200 m around the most active sulphide structure with the highest recorded fluid temperature of over 300°C. The morphology of hydrothermal vents varied greatly from an incipient flat rock with crevices to a 20- to 30-m-tall, multi-flanged structure with concomitant variation in the distribution and abundance of vent-associated megafauna, particularly a galatheid Shinkaia crosnieri and Bathymodiolus mussels. Comparison of active and inactive vents revealed that the spatial extent of Shinkaia ‘aggregation’ (a group of individuals with short nearest-neighbour distances) effectively defined a habitat unit of this species, and active hydrothermal chimneys contained more of these units, leading to greater spatial occupancy by Shinkaia. Given the temporally unstable nature of vent structures as recognised by repeated surveys, vent assemblages are thought to be closely dictated by the spatio-temporal dynamics of vents in the Okinawa Trough back-arc system.
Since the first discovery in the 1970s of organisms associated with deep-sea geothermal activities on the Galapagos Spreading Centre, much research effort has been directed towards gathering information on hydrothermal vents and vent-associated assemblages around the world. Whilst the occurrence of non-vent deep-sea assemblages largely depends upon resources transported from photosynthesis-dominated shallower waters (Gage and Tyler 1991; Gooday 2002; Tokeshi 2002, 2003; Johnson et al. 2007; Galéron et al. 2009; Wei et al. 2010), chemoautotrophic bacterial production dictates the diversity of hydrothermal vent assemblages in different oceanic systems (Parson et al. 1995; Kojima 2002; Van Dover 2000; Nakagawa and Takai 2008). A steadily increasing volume of work on these unique systems has been undertaken, though there is still a paucity of detailed information on the spatio-temporal dynamics and variability of hydrothermal vents and vent-associated assemblages (Lutz and Kennish 1993; Jollivet 1996; Copley et al. 2007; Kato et al. 2010).
While hydrothermal vent assemblages associated with mid-ocean ridge (MOR) systems have been widely known and received much attention (Grassle 1986; Childress and Fisher 1992; Lutz and Kennish 1993; Copley et al. 1997; Gebruk et al. 1997; Tunnicliffe et al. 1998; Desbruyères et al. 2000, 2001; Van Dover 2000; Cuvelier et al. 2009), those associated with non-MOR systems have a shorter research history and, consequently, are scientifically less known. Upwelling of magmas which generates hydrothermal vents in back-arc systems is distinct in that it is associated with episodic or periodic extension of spreading centres, rather than continuous extension as seen in MOR systems (Van Dover 2000; Glasby and Notsu 2003). Thus, hydrothermal vents in a back-arc system constitute a distinct entity that is unrelated in space and time to vents in other systems. Consequently, vent structures in back-arc systems are considered to provide unique examples of varied geomorphological settings for organisms’ existence.
Since their discovery in 1988 (Kimura et al. 1989), the hydrothermal systems in the Okinawa Trough have been the subject of an intensive series of geophysical and biological surveys (e.g. Aoki and Nakamura 1989; Hashimoto et al. 1995; Yamamoto et al. 1999; Fujikura et al. 2001; Ohta and Kim 2001; Watanabe 2001; Glasby and Notsu 2003; Nakagawa et al. 2005) and six active vent fields have been reported to date. These are, from NE to SW, Minami-Ensei Knoll (#1; Fig. 1b), Iheya North (#2), Iheya Ridge (#3), Izena Hole (#4), Hatoma Knoll (#5) and Daiyon-Yonaguni Knoll (#6). All these areas are located along the edges of the rising slope between 700 and 1,500 m depth, while the deepest part of the Trough is formed by a relatively flat, central plain of 1,500–2,000 m depth. The present study deals mainly with the Iheya North area (designated as ‘North Knoll of Iheya Ridge’ in Fujikura et al. 2008) (#2, Fig. 1b) at 950–1,050 m depth in the north-eastern part of the Okinawa Trough where the depth gradient runs from NE (shallower) to SW (deeper). More data are available from this area, as it has been subjected to a series of intensive surveys.
The objective of the present study is to examine the morphological characteristics and spatial patterns of hydrothermally active sulphide structures and vent-associated megafauna, using an extensive collection of photographic and video recordings obtained through manned submersible surveys. In particular, the present study complements the existing physicochemical and microbiological information on the hydrothermal system of Iheya North (Glasby and Notsu 2003; Nakagawa et al. 2005) by presenting photographic records of variable edifice morphologies from the Iheya North area, alongside the analysis of spatial distribution patterns of megafauna on medium to small spatial scales.
2 Materials and methods
The data in the present study consist of video recordings and photographs taken on board the manned submersible “Shinkai 2000” between 1997 and 2002. The submersible was equipped with CCD video and stereo camera systems, both specially adapted for the deep-cruising vehicle and adjusted to photograph the seafloor from different angles. Video recording was carried out continuously throughout a bottom cruise and stereo photographs were taken at either regular (45–60 s; surveys in May 2002) or irregular intervals (all other surveys). Still photographs were also taken from an observation port of the vehicle using a hand-held digital camera, especially when the submersible was temporarily resting on the seabed. A total of over 100 h of video recordings from 20 manned dives, 1,200 high-quality photographs (obtained mainly in the May 2002 survey) and data obtained through unmanned towing surveys were used in the present analysis. All video recordings were reviewed on a high-resolution monitor and parts of the recordings were digitised to obtain still images for cross-comparisons and image analyses on a computer. Similarly, all analogue photographs were also digitised for a computer-based analysis. For the assessment of sulphide structures, still images derived from both analogue/digital photography and video recordings were compared and reconstructed to obtain enlarged and extended images. Occurrence of megafaunal species and hydrothermal vents were carefully noted with reference to the map data obtained through diving operations and deep-tow surveys. In order to facilitate size estimation of objects, video and photographic images often included objects of known sizes such as vehicle parts. In May 2002 surveys, a measuring quadrat (25 × 25 cm) was also deployed. Qualitative samples of benthic organisms were collected using the manipulator and brought back on-board and then to the laboratory for taxonomic and other works.
Two edifice structures of contrasting activity levels (high and low) were chosen for detailed analyses of small-scale spatial patterns of vent assemblages. In the video-reconstructed photographs the edifice surface from the top downwards was covered by 50 × 50 cm grids and the occurrence of organisms (particularly galatheid crabs) in each grid was noted and their two-dimensional cover was quantified as digitised data; these were then used to estimate density and occupancy values [proportion (%) of area occupied]. Density here refers to the minimum estimated value, as those individuals (especially small-sized ones) completely hidden beneath other individuals in a dense aggregation and/or in (parts of) images, where illumination was not sufficient to allow individual recognition, were inevitably overlooked. A total of ca. 300 grids were thus examined for each edifice structure. Further, in order to quantify aggregations of galatheid crabs, an ‘aggregation’ was defined as a group of individuals in which each individual has the first and the second nearest-neighbour distance (NND) of less than half its total body width. The size of an aggregation was thus calculated as area encompassing all the individuals belonging to an aggregation. This working definition is based on the observation that Shinkaia crabs generally formed such a strong concentration in the centre of their local distribution (see Sect. 3). The consideration behind this definition was that (1) one or two isolated individuals cannot be considered as forming aggregation, and (2) only those existing in apparent proximity should be counted as aggregation members, for the definition to be of practical use. Alongside aggregation size, aggregation perimeter length was also measured to assess variation in aggregation pattern, through the examination of area–perimeter relationships using ANCOVA.
3.1 Occurrence of hydrothermal vents
3.2 Mound structures and vent assemblages
Edifice 3 (‘North Big Chimney’) was the most active mound reaching ca. 32 m in height and pyramid-shaped with well-developed, multi-layered flange structures (type 3) (Fig. 4a), with massive aggregations of vent animals, especially towards the peak of the structure. The mound top had an active orifice where hydrothermal fluid gushed out (Fig. 4b), surrounded, at some distance away, by aggregations of Shinkaia crosnieri. Vent organisms included not only invertebrates but also a Zoarcid fish species, which tended to seek shelter in bare patches of sulphide substrate (Fig. 4c). Edifice 4 (‘Central Big Chimney’) was also an active mound with multiple tops and flange structures, covered by massive aggregations of Shinkaiacrosnieri with some patches of vestimentiferan tubeworms (Fig. 5a–e). Edifice 5 (ca. 18 m in height) was similar in morphology to Edifice 2 with multiple mound tops but, unlike Edifice 2, its top parts were covered predominantly by Bathymodiolus mussels with no or few Shinkaia crosnieri, while scattered aggregations of Shinkaia crabs occurred on mound surfaces (Fig. 5f, g). Of the three Bathymodiolus species known to occur in the Okinawa Trough (Fujikura et al. 2008), the materials collected from vent fields of Iheya North during dive No. 1,350 in May 2002 included no specimen of B. aduloides, while B. platifrons accounted for the majority of 128 specimens (ca. 89%) with the rest being identified as B. japonicus. In the samples collected, the less abundant B. japonicus always occurred in mixed patches with B. platifrons without forming a single-species aggregation. In contrast, B. platifrons often achieved near 100% dominance in the areas under study.
3.3 Spatial pattern of vent assemblages
4.1 Spatial distribution and morphology of hydrothermal vents
The occurrence of hydrothermal vents in the Okinawa Trough is apparently non-random and has demonstrated aggregated patterns on different spatial scales. On the scale of 102 to 103 km, i.e. the entire basin, hydrothermal vents were concentrated in the northern and southern parts with no vent being found in the central plain of the Trough (Fig. 1). On the scale of 1–10 km, hydrothermal vents in Iheya North were concentrated within an area of 1 km2 (Fig. 2, upper). Further, on the scale of 102 to 103 m, the majority of vents occurred within a radius of 200 m (Fig. 2, lower), a situation somewhat similar to the occurrence of clusters of sulphur mounds at the Main Endeavour Field of the Juan de Fuca Ridge (Delaney et al. 1992; Robigou et al. 1993) and the PACMANUS site of the Manus Basin (Hashimoto et al. 1999). It is notable here that the occurrence of vents and vent-associated assemblages demonstrated directional, parallel patterns with Edifices 3 and 4 forming the central axis (Fig. 2, lower) and other vents lying on approximately parallel lines. Given the fact that, on the scale of the Okinawa Trough as a whole, the axis of basin expansion runs in the NE to W/SW direction (Glasby and Notsu 2003), it is interesting to note that a similar directionality in hydrothermal activity occurs on a much smaller spatial scale. These patterns of spatial distribution of hydrothermal vents are apparently different from those found in the East Pacific Rise where vent sites occurred in an extensive linear manner (Haymon et al. 1991).
Observations of vent structures in the study area suggest a general sequence of mound development in this system. In the 1st stage, hydrothermal fluid seeps out of fissures in hard, flat substrate and small aggregations of sulphate bacteria, galatheid crabs and bathymodiolid mussels occur around seepages. In the 2nd stage, the accumulation of sulphide material begins with an appearance of incipient flange structures, i.e. the lateral outgrowth of a sulphide mound. The 3rd stage refers to a fully developed edifice with multi-layered flange structures, demonstrated most notably by Edifice 3. Organisms occur all over the edifice walls except underneath a flange shelf where hot liquid tends to accumulate. More animals occur towards the top part of an edifice where vents are more numerous and active, as hot liquid and gas tend to go upwards. The 4th stage shows a degenerative state of mound development where hydrothermal activity is going down (e.g. Edifice 1; Fig. 3) with the erosion and eventual loss of flange structures and declining abundances of vent-associated organisms.
Heterogeneity in vent structures as revealed in the present study is considered to reflect variation in the elapsed time and cycle of hydrothermal activity at particular sites. This also means that, though a general developmental pathway may exist as discussed above, vents do not always follow the same destiny. It has been suggested that massive sulphide structures made of sulphide–anhydrite–silica breccias result from episodes of hydrothermal activity–inactivity, rather than a constant accumulation of sulphides due to continuous hydrothermal activity (Humphris et al. 1995). It is possible that many 1st-stage vents would remain in the same state without further development and disappear with declining hydrothermal activity. In fact, numerous 1st-stage vents occurred as ‘subordinate vents’ on the lower part and walls of an edifice. Therefore, a very small proportion of 1st-stage vents are sufficiently strong and long-lasting to develop into a full-scale sulphide edifice. On the other hand, all vent structures would eventually cease their hydrothermal activity, as the centre of activity gradually but inevitably shifts in position with the expansion of a back-arc basin. Consequently, active vents ‘migrate’ with passage of time, a phenomenon which is thought to underlie the current disjointed distribution of hydrothermal vent sites in the Okinawa Trough. In other words, active vents in the back-arc systems are probably less stable temporally and short-lived on average compared with their counterparts in mid-ocean spreading ridges where the centre of hydrothermal activity is relatively stable in space (see Embley and Chadwick 1994). Thus, hydrothermal vents of a back-arc system are considered to present a highly dynamic environment to their inhabitants, on comparable or smaller scales of time and space as seen in hydrothermal systems of MORs (Fustec et al. 1987; Gebruk et al. 2000a, b; Copley et al. 1997, 2007).
The massive pyramid-shaped structure with fully developed flanges (Edifice 3; Fig. 4) was revealed in its entirety for the first time from the Okinawa Trough in the present analysis. This is of a much larger scale in comparison to a pyramidal flange structure (ca. 2 m high) previously reported from a nearby area (Glasby and Notsu 2003). While this has a clear structural similarity to sulphide mounds found on the Juan de Fuca Ridge (Robigou et al. 1993; Tivey et al. 1999), the broad pyramidal shape rather than a tall chimney shape of the whole construct suggests that the deposition of sulphide material in this system has been slower than in most mid-ocean hydrothermal systems where simple columnar chimneys commonly occur along fast-spreading ridges (Wilcock and Delaney 1996). The fact that shimmering fluid was often visible on the upper side of a flange and that macrofauna tended to be sparse on the upper side of a horizontally expanding flange structure suggests that the elevated temperature occurring there (see Woods and Delaney 1992) may be inhospitable to invertebrates. An experiment under high pressure conditions (Lee 2003) indicated that the temperature tolerance of deep-sea metazoan life would be under 60°C.
Even if the position of a vent and its level of hydrothermal activity do not appreciably change over a relatively short period of time (e.g. several weeks to several years), the physical structure of a sulphide mound is constantly changing. This is due to the fact that sulphide structures, especially surface projections such as chimney tops and flanges, are mechanically weak and their increasing weight and volume cannot permanently be supported. Similarly, in the case of vents with decreasing hydrothermal activity, the accumulation of new sulphide deposits is less than what is being lost by gradual erosion of surface structures. In the present study, a lateral projection (part of a flange, ca. 1 m length × 1 m height) on the top part of Edifice 3 was apparently lost sometime between 1999 and 2002, with a concomitant loss of a colony of vestimentiferan tubeworms (the largest aggregation on Edifice 3) that was observed in earlier surveys. This clearly indicates that sulphide mounds undergo constant morphological changes that would affect the development of vent-associated assemblages.
4.2 Vent structures and their assemblages
The hydrothermal vent assemblages of the Okinawa Trough are characterised uniquely by the dominance of a galatheid Shinkaia crosnieri (Baba and Williams 1998) around virtually all active vents (this study; Kimura et al. 1989; Fujikura et al. 2001). While galatheid crabs are common in both deep-sea hydrothermal and non-hydrothermal habitats (e.g. Gage and Tyler 1991; Desbruyères and Segonzac 1997; Van Dover 2000; Tokeshi 2003), dense aggregations of galatheids seem to characterise in particular high-temperature vents of the Okinawa Trough (e.g. observations in Hatoma and Dai-yon Yonaguni Knolls; Tsuchida et al. 2003). In hydrothermal systems of the East Pacific Rise and the Northeast Pacific Ridges, vestimentiferan tubeworms formed dense aggregations around vent orifices (Fustec et al. 1987; Sarrazin and Juniper 1999; Tsurumi and Tunnicliffe 2003), while in Mid-Atlantic and Indian Ocean hydrothermal systems aggregations of free-swimming rimicarid shrimps characterised active diffusers (Gebruk et al. 1997; Segonzac 1992; Segonzac et al. 1992; Polz et al. 1998; Van Dover et al. 1996, 2001; Hashimoto et al. 2001; Copley et al. 2007).
Amongst decapod crustaceans, bythograeid crabs have been reported as being closely associated with hydrothermal vents on the East Pacific Rise (Bythograea thermydron, Williams 1980) the back-arc basins of western Pacific (Mariana: Austinograea williamsi, Hessler and Lonsdale 1991; Manus and Lau: A. alayseae, Desbruyères and Segonzac 1997; Izu-Ogasawara: Gandalfus yunohana, Hashimoto and Fujikura 1992) and also the Mid-Atlantic Ridge (Segonzacia mesatlantica, Desbruyères and Segonzac 1997; Cuvelier et al. 2009). The spatial aggregations of these bythograeid crabs, however, do not seem to reach the magnitude observed for Shinkaiacrosnieri in the Okinawa Trough.
Apart from tube worms and crustaceans, bathymodiolid mussels are common and often achieve a high abundance in most hydrothermal vent systems around the world (Gebruk et al. 2000a; Van Dover 2002; Cuvelier et al. 2009). On the other hand, bathymodiolids do not normally occur very close to an active vent orifice but some distance from it (note, however, the report by Cuvelier et al. 2009 documenting the occurrence of Bathymodiolus azoricus aggregations close to fluid exits at Lucky Strike, MAR), as observed in the present study for Bathymodiolus platifrons with its distribution extending to the periphery of a vent. This may reflect their lower tolerance levels of temperature and/or hydrogen sulphide than aggregation-forming tubeworms (Lee 2003).
The observed spatial arrangements of the two large-sized macroinvertebrates that characterise hydrothermal vent assemblages of the Okinawa Trough (this study; Fujikura et al. 2001) reflect the underlying spatial pattern of hydrothermal activity. In particular, Shinkaia aggregations were invariably observed in places where a visible shimmering of hydrothermal fluids occurred. As free-ranging animals, Shinkaia crabs appear to have a clear advantage over sessile Bathymodiolus in colonising vent habitats, similar to a free-ranging rimicarid Rimicaris exoculata in Mid-Atlantic systems (Segonzac 1992; Segonzac et al. 1992). In hydrothermal vents, physicochemical aspects including the flow regimes of hydrothermal fluids, temperature and hydrogen sulphide concentrations are highly variable in space and time, leading to high variability in faunal abundance and distribution (Hessler et al. 1985; Fustec et al. 1987; Segonzac 1992; Chevaldonné and Jollivet 1993; Van Dover et al. 1996; Copley et al. 1997, 2007; Sarrazin et al. 1997, 1999; Sarrazin and Juniper 1999; Gebruk et al. 2000a, b). In such variable environments, mobile Shinkaiacrosnieri is well-adapted for forming aggregations in optimum microhabitats, as demonstrated by their pattern of spatial occupancy on edifices of contrasting activity levels (Fig. 7). Thus, Shinkaiacrosnieri formed strong aggregations in hydrothermally active sites with their abundances closely reflecting the strength of hydrothermal activity. This also agrees with the observation that Shinkaia crosnieri did not aggregate around a relatively low-temperature vent under an artificial rearing condition (Miyake et al. 2007).
The predominance of Shinkaiacrosnieri with Bathymodiolus mussels in the Okinawa Trough makes a contrast to hydrothermal vent systems of the Eastern Pacific where vestimentiferan tubeworms are predominant around active orifices, especially at early stages of vent development (Desbruyères 1995; Fustec et al. 1987; Tsurumi and Tunnicliffe 2001, 2003). This gives credence to the view that the faunal assemblages of the Okinawa Trough constitute a biogeographically distinct entity, largely due to the fact that the Okinawa Trough is tectonically separate from MOR systems. This in turn points to the importance of plate tectonics in the formation of hydrothermal vent faunas (Tunnicliffe and Fowler 1996; Tunnicliffe et al. 1998). The rapid colonisation of a vent site by vestimentiferans as observed in the East Pacific Rise (Shank et al. 1998) seems to be replaced in the Okinawa Trough by Shinkaia crabs capable of making quick responses to vent appearance. It may be hypothesised that their tendency to make dense aggregations (‘patches’) around a vent orifice hinders colonisation by vestimentiferans in this system. Further, aggregations of Bathymodiolus could also hinder vestimentiferan colonisation. It remains to be seen whether such spatial interactions as observed for sessile intertidal assemblages (Tokeshi 1999) could account for the relatively low abundance (i.e. lack of large aggregations, though they are commonly observed as scattered patches/individuals in all types of vent environments) of vestimentiferans in the hydrothermal vent systems of the Okinawa Trough.
Hydrothermal vents in the Okinawa Trough back-arc system had varied spatial structures on regional to local scales, including the morphological variability of sulphide edifices. These structural variations coupled with the changing pattern of hydrothermal activity were closely accompanied by variation in vent-associated assemblages, particularly an endemic galatheid Shinkaia crosnieri and bathymodiolid mussels. Comparative geomorphological and biogeographical studies of different vent structures may give further insight into the workings of these unique hydrothermal systems.
Thanks are due to the Captain of the support vessel “Natsushima”, Mr. F. Saito, the Commander, Mr. Y. Yoda, and the piloting team of the “Shinkai 2000” submersible (in particular the Pilots, Messrs K. Matsumoto, H. Ueki and Y. Oono) and other crew members for unstinting logistical support during the research cruise in May 2002 during which a major portion of the data used in the present article was gathered. Thanks are also due to Dr K. Fujikura of the Japan Agency for Marine-Earth Science and Technology for providing video records and related data of past diving surveys and all those involved in “Shinkai 2000” surveys until the submersible ceased its active operation in November 2002. I am also indebted to members of the Amakusa Marine Biological Laboratory for various forms of help with data processing and manuscript preparation. This work was supported in part by the P&P programs and the GCOE program of the Kyushu University and by “the Grants-In-Aid for Scientific Research” (Nos. 14255013, 14340246) from the Japan Society for the Promotion of Science.