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Supplementary Information
Where are the undiscovered hydrothermal vents on oceanic spreading ridges?
Stace E. Beaulieua*, Edward T. Bakerb, and Christopher R. Germana
a Woods Hole Oceanographic Institution, Woods Hole, MA 02543 USA (* [email protected])
b Joint Institution for the Study of the Atmosphere and Ocean—PMEL, University of
Washington, Seattle WA 98115 USA
29 January 2015
22 pages (including cover page)
Supp. Methods
Supp. Discussion
Supp. References
1 Supp. Data file (separate file)
1 Supp. Figure
2 Supp. Tables
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Supplementary Methods
Calculating strike length surveyed for hydrothermal activity
Estimates of total strike length for mid-ocean ridges (MORs) and back-arc spreading centers
(BASCs) in the literature vary depending on the model used for divergent plate boundaries and
whether or not to include certain categories of spreading such as continental rifts. The total
spreading ridge strike length used in this global analysis (71,284 km) is calculated by assigning
every submarine oceanic spreading ridge (OSR) “digitization step” (66,908 km) and a subset of
continental rift boundary (CRB) steps (4,376 km) in the PB2002 model (Bird, 2003) to MOR or
BASC regions (Supp. Data; note: plate identifiers are provided in the Supp. Data caption below).
A digitization step is defined as “the short great circle arc between adjacent digitized plate
boundary points” (Bird, 2003). We retain the word “step” when referring to our use of the
PB2002 model, to distinguished from ridge “segment” and surveyed “portions” of ridges. The
subset of CRB steps is mainly three regions with known vents (Bransfield Strait, Okinawa
Trough, and Red Sea) and also smaller lengths contained within a series of OSR steps [e.g., in
Lau Basin, the Mangatolu Triple Junction (MTJ) portion of TO-NI boundary and Lau
Extensional Transform Zone (LETZ) portion of NI-AU boundary]. The MOR strike length
(60,139 km, 84% of total spreading ridge) matches the previous review (Baker and German,
2004), while the BASC strike length (11,145 km, 16% of total spreading ridge) is ~4,000 km
longer. The MOR strike length includes the ultraslow-spreading OSR steps on NA-SA (992 km)
and IN-AU (1059 km) (Supp. Table 1), new plate boundaries as determined by seismicity (Bird,
2003).We note that the more recent NNR-MORVEL56 model (Argus et al., 2011) includes four
more plates, but plate boundaries “are merely a minor update to those of Bird (2003).”
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To determine the total strike length within and outside exclusive economic zones (EEZs) (Supp.
Table 2), we applied a “point in polygon” algorithm (modified from
http://www.nceas.ucsb.edu/scicomp/usecases/point-in-polygon) to the start and end positions of
each submarine OSR and CRB step used from the PB2002 model (Bird, 2003) against EEZ
polygons in the Maritime Boundaries Geodatabase (VLIZ, 2009). Positions given as high seas in
this database translate to The Area (the seafloor beyond the limits of national jurisdiction) and
extended continental shelves at the seafloor. Presently, applications for extended continental
shelves outside of EEZs are still being submitted by states to the United Nations Commission on
the Limits of the Continental Shelf; thus, we can only report our estimates within and outside
EEZs in terms of national jurisdiction. For the few instances when either the start or end position
fell within an EEZ and the other was high seas, the full step was counted in the EEZ strike length
(thus, in a few cases there could be a slight over-estimate when a step straddled the EEZ
boundary). For the few instances in which the start and end fell within different EEZs (e.g., Red
Sea and Lau Basin Futuna Spreading Center), each step was assigned to national jurisdiction
based on having a majority of its length within a particular EEZ.
To determine the strike length of spreading ridges surveyed for hydrothermal activity, we
identified the subset of OSR and CRB steps corresponding to every published systematic survey
(Supp. Data), with the exception of Mohns Ridge for which we used 10% of its total strike length
(Pedersen et al., 2010). The original intention with cataloging hydrothermal surveys was to
identify those surveys long enough and dense enough to contribute to a global correlation of
plume incidence (fraction of ridge crest over which a plume anomaly is observed in the water
column) or vent field frequency (at the seafloor) to spreading rate (e.g., > 200 km and densely or
moderately surveyed; (Baker and German, 2004)). Survey density is described fully by Baker
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and German (2004); briefly: dense refers to continuous (e.g., by a towed instrument package) or
closely-spaced (e.g., vertical profiles < ~10 km apart) mapping of hydrothermal plumes,
moderate represents discrete mapping of plumes and/or seafloor deposits with less dense spacing
(e.g., vertical profiles > ~10 km apart), and sparse indicates discrete mapping with spacing too
far apart to achieve a representative sampling of a continuous plume distribution in the water
column or to assess the distribution of seafloor deposits. The re-analysis of surveyed strike
lengths as of year 2001 using the PB2002 model (Bird, 2003) matched well with the previous
review with a total of 14,585 km (Supp. Table 1; compare to 13,300 in (Baker and German,
2004), plus ~1000 km more sparsely surveyed in (Baker et al., 1995)). This review adds 8731
km of surveys in the decade from ~2001-2010, bringing the total strike length at least sparsely
surveyed to 23,316 km (Supp. Table 1). Most of this total surveyed length is moderately or
densely surveyed (20,229 km). We thank those private companies and national jurisdictions who
shared their data from systematic surveys for hydrothermal plumes and seafloor massive sulfide
deposits.
An asterisk in Supp. Table 1 indicates that additional systematic surveys have been performed in
the region since ~2010. In general publications are not yet available for these very recent
surveys, listed here by region, year, and cruise: Chile Rise, 2010, INSPIRE; Galápagos
Spreading Center: 2009, R/V Dayang Yihao DY115-21, and 2011, GALREX; Gulf of California,
2012, Monterey Bay Aquarium Research Institute; Red Sea, 2012, PELAGIA 64PE350;
Southeast Indian Ridge (SEIR), 2011-2013, Korea Polar Research Institute; Southwest Indian
Ridge (SWIR), 2010 and 2011, R/V Dayang Yihao; Lau Basin Futuna Spreading Center, 2010
and 2012, IFREMER (MNF-ss2012_v02); Lau Basin NELSC and Eastern Lau Spreading Center
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(ELSC) and Havre Trough, 2010, Korea Ocean Research and Development Institute; Mid-
Atlantic Ridge 13-33 S, 2013, R/V Merian MSM25.
Methods for new linear fit of vent field frequency to spreading rate
An equation for the linear relationship of spatial density, or frequency (Fs) of vent fields per 100
km spreading ridge, to weighted average full spreading rate (us) was published in the previous
global compilation of hydrothermal surveys on spreading ridges (Baker and German, 2004) and
revised by (Baker et al., 2004). More recent publications only included equations for the linear
relationship of hydrothermal plume incidence to spreading rate or magma budget (e.g., Baker et
al., 2008b). Here, we report as Eq. 1 a revised linear fit for vent field frequency to spreading rate
including the previous 12 (with SEIR extended) and 9 new non-hotspot, moderately-to-densely
surveyed portions :
Fs = 0.95 + 0.020 us (Eq. 1)
(R2 = 0.47; “21-pt linear regression” in Fig. 3A). Although there is scatter, expected due to
variability in survey effort and discrimination of vent field locations (Baker et al., 2004), the
correlation for the 21 data points is significant (r = 0.68, p = 0.0007) We also report here as Eq. 2
the linear fit for all 27 surveys in Table 1A including hotspot-influenced portions of MORs and
the Lau ELSC/Valu Fa Ridge (VFR):
Fs = 0.85 + 0.023 us (Eq. 2)
(R2 = 0.27; “27-pt linear regression” in Fig. 3A). The correlation for the 27 data points is
significant (r = 0.5209, p = 0.005). Hotspot-affected regions were excluded in previous
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publications for the linear fit of vent field frequency to spreading rate (Baker and German, 2004;
Baker et al., 2004; Dyment et al., 2007; Baker et al., 2008b). The Lau ELSC/VFR has by far the
highest observed Fs of any spreading ridge and is grossly affected by arc magma (Baker et al.,
2006; Martinez et al., 2006). All listings in Table 1A were surveyed with sufficient density and
length (> 200 km) and with data available for vent field locations; additional listings in Table 1B
that were moderately or densely surveyed for > 200 km may be included in future iterations of
the linear fit with publication of and/or access to more data.
In previous publications for this linear relationship, to achieve a minimum ridge length of > 500
km for each data point and reduce scatter (Baker and German, 2004; Baker et al., 2004), data
were binned into five spreading rate categories: ultraslow (0-20 mm/yr), slow (20-55 mm/yr),
intermediate (55-80 mm/yr), fast (80-140 mm/yr), and superfast (>140 mm/yr). For comparison,
we binned the 21non-hotspot portions into the same five spreading rate categories (Fig. 3B) and
report the binned fit:
Fs = 0.85 + 0.021 us (Eq. 3)
(R2 = 0.88; greater coefficient of determination than Eq. 1). The correlation for the binned data
points is significant (r = 0.94, p-value 0.018). Binned values use reported and/or measured
lengths (i.e., summing the vent fields in the non-contiguous portions and plotting against
weighted average spreading rate). All three new equations have similar intercepts but slightly
greater slope than the most recently published equation (Fs = 0.98 + 0.015 us; Baker et al., 2004).
We note that at fast spreading rates the new binned fit (Eq. 3) just exceeds the 95% confidence
limit in Baker et al. (2004; their Fig. 21b).
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For vent field locations we used the InterRidge Global Database of Active Submarine
Hydrothermal Vent Fields (InterRidge Vents Database), Version 2.1, with updates as described
in (Beaulieu et al., 2013). We excluded off-axis vent fields, and we combined two original
listings into one on SWIR 58.5-66° E. In addition, for the most recent surveys (vent fields not yet
in the database) we added 8 vent fields to Lau NELSC/MTJ (E. Baker, unpub. data), 9 to the
Central Indian Ridge 8-17° S (Son et al., 2014) and 31 to the SEIR (Baker et al., 2014). We
included confirmed and inferred active vent fields from the database, with “confirmed” meaning
ground-truthed with observations at the seafloor and “inferred” usually meaning that a
hydrothermal plume was detected in the water column and the location for venting at the seafloor
was estimated. We note that confirmed active vent fields categorized as “low-temperature” or
with measured fluid temperatures < 100° C contribute to the Fs value in several of the data points
in the scatterplot (Fig. 3A). Vent fields that are inferred active from hydrothermal plume surveys
using MAPRs and/or optical backscatter are likely to be high-temperature (i.e., black-smoker).
Modern oxidation-reduction potential (ORP)-equipped MAPRs could detect low-temperature
vent fields (Walker et al., 2007), especially if deployed close to the seafloor (e.g., in association
with imaging survey).
In Table 1A we provide the vent field frequency for each survey length, using both the modeled
step lengths (Bird, 2003) and reported survey lengths and/or measured lengths from bathymetry
in the Global Multi-Resolution Topography (GMRT) synthesis (Ryan et al., 2009) accessed via
GeoMapApp software (http://www.geomapapp.org). In general the modeled length was slightly
higher than the (contained) measured length, and thus, resulted in slightly less Fs.
The surveyed regions used in the “21-pt” and “binned” linear fits account for 12313 km
(modeled; 11763 km measured), or 17% of global spreading ridge strike length. This subset is
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quite representative of global spreading ridges with 90% MOR and 10% BASC (compared to
84% MOR and 16% BASC globally) and 53 mm/yr weighted average spreading rate (compared
to 46 mm/yr in this global analysis). To obtain weighted average spreading rate for each portion
of surveyed ridge, we multiplied length and spreading rate for each step in the PB2002 model
(Bird, 2003), summed those results and then divided by the total modeled length of the surveyed
portion. The 21 data points in Fig. 3A were binned as follows: ultraslow (n=5, combined 2534
km modeled, 21% of total length used in linear fit), slow (20-55 mm/yr, although all data were
within 20-40 mm/yr, n=7, combined 4120 km modeled, 33%), intermediate (55-80 mm/yr, n=4,
combined 3253 km modeled, 26%), fast (80-140 mm/yr, although all data were within 80-110
mm/yr, n=3, combined 1279 km, 10%), and superfast (>140 mm/yr, n=2, combined 1127 km,
9%). Again, we note that this is a representative subset of the global ridge crest, as the
percentage contributions to the total strike length match well with the global model (% of strike
length in this global analysis: ultraslow 26%, slow 38%, intermediate 22%, fast 11%, superfast
3%). We note that as a consequence of using the PB2002 model for spreading rates, N EPR 15.5-
18.5° N is grouped into the intermediate spreading rate category [previously assigned to fast
spreading in Baker and German (2004)].
Using the global weighted average full spreading rate (46 mm/yr), the binned fit Eq. 3 yields a
global average Fs of 1.8 (with 95% confidence limits 1.0-2.6), and multiplied by total strike
length predicts a total of 1305 active vent fields on spreading ridges (with 95% confidence limits
713-1853). Interestingly, this matches well with the range (~800-1600) proposed by German et
al. (2011), inclusive of high and low temperature vent fields. Here we explain why our predicted
total number is consistent with (although exceeds) the prediction from the previous review
(1060, with 95% confidence limits 992-1153; (Baker and German, 2004)). First, although we are
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using a value similar to the previous review for global average spreading rate, we are including
approximately 6% more strike length, which would increase the predicted number of vent fields
to 1120. Second, the equation in the previous review (Fs = 0.88 + 0.015 us) was revised (Baker et
al., 2004) (Fs = 0.98 + 0.015 us), and plugging global us into the revised equation yields a global
average Fs of 1.7 (as reported in (Baker et al., 2008a)), and multiplied with the strike length in
this global analysis predicts 1191 vent fields. Third, for the 12 surveyed regions binned in
(Baker and German, 2004) and (Baker et al., 2004), our current values for Fs are slightly higher
because we now know of more vent fields in these regions as compared to a decade ago due to
additional discoveries (e.g., SEIR). We binned and re-calculated the linear regression for just
these 12 regions (Fs = 1.28 + 0.017 us), and the re-calculated prediction of total population of
vent fields was 1476 (higher than our current prediction using Eq. 3). We also note that the total
and 95% confidence interval for our predicted population of vent fields on spreading ridges are
consistent with the total (~900) and range (~500 - 5000) of high-temperature hydrothermal
deposits estimated using a very different method independent of spreading rate (Hannington et
al., 2011).
Supplementary Discussion
Additional regions intriguing for exploration
Other ultraslow- and slow-spreading MOR regions that are intriguing for exploration include the
Red Sea, Ayu Trough, Sorol Trough, and American-Antarctic Ridge. Although the Red Sea was
the first region to be known for deep seafloor hydrothermal activity, perhaps dating back to the
1880's (Miller et al., 1966), the first systematic hydrothermal survey was just completed in 2012
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(cruise PELAGIA 64PE350). Of the 6 small plates in the PB2002 model (Bird, 2003) with no
known vents on any boundaries (only 3 of which have submarine OSR steps), the Caroline (CL)
plate is an interesting target for exploration, including the ultraslow (and perhaps extinct?)
spreading ridges of the Ayu Trough and Sorol Trough, the latter of which is tantalizing as its
location (in Micronesia EEZ) is about halfway between known vents in the Mariana Trough and
Manus Basin (separated by almost 2000 km) and could be an important stepping stone in
present-day biogeography of vent fauna. The ultraslow American-Antarctic Ridge (AN-SA plate
boundary) has yet to be explored for vents which may confirm the new biogeographic province
suggested for Antarctic vent fauna (Rogers et al., 2012). Some of the ultraslow and slow
spreading OSR steps on otherwise transform boundaries are also intriguing to consider for future
exploration in the context of biogeography, for example at high latitudes on the South Scotia
Ridge (SC-AN, Antarctic 200NM zone) and Macquarie Ridge Complex (PA-AU, Australia -
Macquarie Island EEZ).
In terms of other BASC regions that are intriguing for exploration, at ultraslow spreading rates
we highlight the boundaries of Amur (AM) and Anatolia (AT), the two remaining small plates
with submarine OSR steps but no known vents. These plate boundaries, AM-ON in Japan’s EEZ
and AT-AS in the EEZs of Turkey and Greece, respectively, have relatively short lengths of
spreading ridge with close access to ports. There is also a “jog” with ultraslow spreading in the
otherwise convergent boundary at the North Scotia Ridge (SC-SA), of interest to explore for
vent-endemic fauna similar to the new biogeographic province proposed for the East Scotia
Ridge (Rogers et al., 2012). At faster spreading rates, the TO-NI, PA-NI, and NI-FT plate
boundaries are targets in the Lau Basin, and in Manus Basin targets include NB-SB and MN-SB
(the Southern Rifts), known for active volcanism albeit with observations suggesting a low
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magmatic budget (Sinton et al., 2003). In the North Fiji Basin plate boundaries with spreading
rates 100-140 mm/yr are CR-NH and a short strike length at the easternmost (NH-AU) boundary,
an incipient rift at the southern end of the Hunter Ridge (although MAPRs on dredges to that
location did not indicate activity in 2009; L. Danyushevsky, pers. comm.). At intermediate-
spreading rates, a short length of the Woodlark-Birds Head (WL-BH) boundary, in a complicated
region of extensional tectonism (see recent review (Baldwin et al., 2012)), also has no known
vents (Indonesia EEZ).
Other EEZs lacking systematic hydrothermal surveys that also have no known vents include (in
descending order of total strike length), Norway - Bouvet Island (mainly SWIR), Palau (Ayu
Trough), South Africa - Prince Edward Islands (mainly SWIR), and Brazil (N MAR) (Supp.
Table 2).
Supplementary References
Argus, D.F., Gordon, R.G., DeMets, C., 2011. Geologically current motion of 56 plates relative to the no-net-rotation reference frame. Geochemistry, Geophysics, Geosystems 12 (11), Q11001.
Baker, E.T., Edmonds, H.N., Michael, P.J., Bach, W., Dick, H.J.B., Snow, J.E., Walker, S.L., Banerjee, N.R., Langmuir, C.H., 2004. Hydrothermal venting in magma deserts: The ultraslow-spreading Gakkel and Southwest Indian Ridges. Geochemistry, Geophysics, Geosystems 5 (8), Q08002, doi: 10.1029/2004GC000712.
Baker, E.T., Embley, R.W., Walker, S.L., Resing, J.A., Lupton, J.E., Nakamura, K.-i., de Ronde, C.E.J., Massoth, G.J., 2008a. Hydrothermal activity and volcano distribution along the Mariana arc. J. Geophys. Res. 113 (B8), B08S09, doi: 10.1029/2007JB005423.
Baker, E.T., Haymon, R.M., Resing, J.A., White, S.M., Walker, S.L., Macdonald, K.C., Nakamura, K.-i., 2008b. High-resolution surveys along the hot spot–affected Galápagos Spreading Center: 1. Distribution of hydrothermal activity. Geochemistry, Geophysics, Geosystems 9 (9), Q09003, doi: 10.1029/2008GC002028.
Baker, E.T., German, C.R., 2004. On the global distribution of hydrothermal vent fields. In: German, C.R., Lin, J., Parson, L.M. (Eds.), Mid-Ocean Ridges: Hydrothermal Interactions
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231232233
234235236237
238239240
241242243244
245246
Between the Lithosphere and Oceans. American Geophysical Union, Washington, D.C., pp. 245-266, doi: 10.1029/148GM10.
Baker, E.T., German, C.R., Elderfield, H., 1995. Hydrothermal plumes over spreading-center axes: Global distributions and geological inferences. In: Humphris, S., Zierenberg, R., Mullineaux, L.S., Thomson, R. (Eds.), Seafloor hydrothermal systems: Physical, chemical, biological, and geological interactions. American Geophysical Union, Washington, D.C., pp. 47-71, doi: 10.1029/GM091p0047.
Baker, E.T., Hemond, C., Briais, A., Maia, M., Scheirer, D.S., Walker, S.L., Wang, T., Chen, Y.J., 2014, in press. Correlated patterns in hydrothermal plume distribution and apparent magmatic budget along 2500 km of the Southeast Indian Ridge. Geochem. Geophys. Geosyst. , doi: 10.1002/2014GC005344.
Baker, E.T., Resing, J.A., Walker, S.L., Martinez, F., Taylor, B., Nakamura, K., 2006. Abundant hydrothermal venting along melt-rich and melt-free ridge segments in the Lau back-arc basin. Geophysical Research Letters 33 (7), L07308, doi: 10.1029/2005GL025283.
Baldwin, S.L., Fitzgerald, P.G., Webb, L.E., 2012. Tectonics of the New Guinea Region. Annual Review of Earth and Planetary Sciences 40 (1), 495-520, doi: 10.1146/annurev-earth-040809-152540.
Beaulieu, S.E., Baker, E.T., German, C.R., Maffei, A., 2013. An authoritative global database for active submarine hydrothermal vent fields. Geochemistry, Geophysics, Geosystems 14 (11), 4892-4905, doi: 10.1002/2013GC004998.
Bird, P., 2003. An updated digital model of plate boundaries. Geochemistry, Geophysics, Geosystems 4 (3), 1027, doi: 10.1029/2001GC000252.
Dyment, J., Lin, J., Baker, E.T., 2007. Ridge-hotspot interactions: What mid-ocean ridges tell us about deep Earth processes. Oceanography 20 (1), 102-115, http://dx.doi.org/10.5670/oceanog.2007.84.German, C.R., Ramirez-Llodra, E., Baker, M.C., Tyler, P.A., et al., 2011. Deep-Water Chemosynthetic Ecosystem Research during the Census of Marine Life Decade and Beyond: A Proposed Deep-Ocean Road Map. PLoS ONE 6 (8), e23259, doi: 10.1371/journal.pone.0023259.
Hannington, M., Jamieson, J., Monecke, T., Petersen, S., Beaulieu, S., 2011. The abundance of seafloor massive sulfide deposits. Geology 39 (12), 1155-1158, doi: 10.1130/G32468.1.
Martinez, F., Taylor, B., Baker, E.T., Resing, J.A., Walker, S.L., 2006. Opposing trends in crustal thickness and spreading rate along the back-arc Eastern Lau Spreading Center: Implications for controls on ridge morphology, faulting, and hydrothermal activity. Earth and Planetary Science Letters 245 (3–4), 655-672, doi: 10.1016/j.epsl.2006.03.049.
Miller, A.R., Densmore, C.D., Degens, E.T., Hathaway, J.C., Manheim, F.T., McFarlin, P.F., Pocklington, R., Jokela, A., 1966. Hot brines and recent iron deposits in deeps of the Red Sea. Geochimica et Cosmochimica Acta 30 (3), 341-359, doi: 10.1016/0016-7037(66)90007-X.
Pedersen, R.B., Thorseth, I.H., Nygård, T.E., Lilley, M.D., Kelley, D.S., 2010. Hydrothermal Activity at the Arctic Mid-Ocean Ridges. In: Rona, P.A., Devey, C.W., Dyment, J., Murton, B.J. (Eds.), Diversity Of Hydrothermal Systems On Slow Spreading Ocean Ridges. American Geophysical Union, Washington, D.C., pp. 67-89, doi: 10.1029/2008GM000783.
12
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254255256257
258259260
261262263
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269270271272273274
275276
277278279280
281282283
284285286287
Rogers, A.D., Tyler, P.A., Connelly, D.P., Copley, J.T., James, R., Larter, R.D., Linse, K., Mills, R.A., Garabato, A.N., Pancost, R.D., Pearce, D.A., Polunin, N.V.C., German, C.R., Shank, T., Boersch-Supan, P.H., Alker, B.J., Aquilina, A., Bennett, S.A., Clarke, A., Dinley, R.J.J., Graham, A.G.C., Green, D.R.H., Hawkes, J.A., Hepburn, L., Hilario, A., Huvenne, V.A.I., Marsh, L., Ramirez-Llodra, E., Reid, W.D.K., Roterman, C.N., Sweeting, C.J., Thatje, S., Zwirglmaier, K., 2012. The Discovery of New Deep-Sea Hydrothermal Vent Communities in the Southern Ocean and Implications for Biogeography. PLoS Biol 10 (1), e1001234, doi: 10.1371/journal.pbio.1001234.
Ryan, W.B.F., Carbotte, S.M., Coplan, J.O., O'Hara, S., Melkonian, A., Arko, R., Weissel, R.A., Ferrini, V., Goodwillie, A., Nitsche, F., Bonczkowski, J., Zemsky, R., 2009. Global Multi-Resolution Topography synthesis. Geochem. Geophys. Geosyst. 10, Q03014, doi: 10.1029/2008GC002332.
Sinton, J.M., Ford, L.L., Chappell, B., McCulloch, M.T., 2003. Magma Genesis and Mantle Heterogeneity in the Manus Back-Arc Basin, Papua New Guinea. Journal of Petrology 44 (1), 159-195, doi: 10.1093/petrology/44.1.159.
Son, J., Pak, S.-J., Kim, J., Baker, E.T., You, O.-R., Son, S.-K., Moon, J.-W., 2014. Tectonic and magmatic control of hydrothermal activity along the slow-spreading Central Indian Ridge, 8°S-17°S. Geochemistry, Geophysics, Geosystems 15 (5), 2011-2020, doi: 10.1002/2013GC005206.
VLIZ, 2009. Maritime Boundaries Geodatabase, World EEZ version 5, released 2009-10-01, available online at http://www.marineregions.org/downloads.php#eez.
Walker, S.L., Baker, E.T., Resing, J.A., Nakamura, K., McLain, P.D., 2007. A New Tool for Detecting Hydrothermal Plumes: an ORP Sensor for the PMEL MAPR. American Geophysical Union, Fall Meeting, abstract #V21D-0753.
Supplementary Data file. All submarine oceanic spreading ridge (OSR) and a subset of
continental rift boundary (CRB) steps in PB2002 model (Bird, 2003) assigned to region,
national jurisdiction, and systematic hydrothermal survey. We provide an ascii txt data file
with 14 columns and 1969 rows, including the following column headers: 1) step number in
PB2002 model (Bird, 2003); 2) step class (OSR or CRB); 3) plate boundary (AF Africa, AM
Amur, AN Antarctica, AP Altiplano, AR Arabia, AS Aegean Sea, AT Anatolia, AU Australia,
BH Birds Head, BR Balmoral Reef, BS Banda Sea, BU Burma, CA Caribbean, CL Caroline, CO
Cocos, CR Conway Reef, EA Easter, EU Eurasia, FT Futuna, GP Galápagos, IN India, JF Juan
de Fuca, JZ Juan Fernandez, KE Kermadec, MA Mariana, MN Manus, MO Maoke, MS Molucca
13
288289290291292293294295
296297298299
300301302
303304305306
307308
309310311
312
313
314
315
316
317
318
319
320
321
Sea, NA North America, NB North Bismarck, ND North Andes, NH New Hebrides, NI
Niuafo'ou, NZ Nazca, OK Okhotsk, ON Okinawa, PA Pacific, PM Panama, PS Philippine Sea,
RI Rivera, SA South America, SB South Bismarck, SC Scotia, SL Shetland, SO Somalia, SS
Solomon Sea, SU Sunda, SW Sandwich, TI Timor, TO Tonga, WL Woodlark, YA Yangtze); 4)
longitude at start of step (decimal degrees); 5) latitude at start of step (decimal degrees); 6)
longitude at end of step (decimal degrees); 7) latitude at end of step (decimal degrees); 8) step
length (km); 9) full spreading rate at midpoint of step (mm/a); 10) tectonic setting (MOR or
BASC); 11) region used in InterRidge Vents Database (Beaulieu et al., 2013); 12) national
jurisdiction (VLIZ, 2009); 13) new survey indicator [0 if no survey, 1 if survey in (Baker et al.,
1995) and/or (Baker and German, 2004), 2 if survey added in this paper]; 14) current survey type
(1 is densely surveyed, 2 moderately, 3 sparsely). Note that surveys for the Mohns Ridge could
not be assigned to model steps, thus the total strike length surveyed in this data file is 23,238 km
(78 km less than 23,316 km in Supp. Table 1).
Supplementary Figure Legend
Supp. Fig 1. Strike length remaining to be surveyed and number of undiscovered vent
fields within EEZs per national jurisdiction. Surveyed strike lengths (A) and predicted
numbers of undiscovered vent fields (B) per national jurisdiction, arranged alphabetically with
inset for outside EEZs.
14
322
323
324
325
326
327
328
329
330
331
332
333
334
335
336
337
338
339
340