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Regional arrays of borehole observatories for sustained time-series observations of (a)subseafloor hydrogeological processes and (b) formation pressure as proxy for plate-scale strain

1.0 Introduction

Deep ocean boreholes provide unique opportunities for determining the physical,chemical, and biological state and properties of sub-seafloor formations. Eighteen holes drilledby the Ocean Drilling Program (ODP) were completed with "CORK" (Circulation ObviationRetrofit Kit) instrumentation during 1991-2003 for long-term formation temperature andpressure monitoring, fluid sampling, and active hydrologic testing (e.g., Davis and Becker, 2001;Becker and Davis, in press; CORK bibliography at end of references cited). Three newinstallations completed during the first phase of the Integrated Ocean Drilling Program (IODP)in 2004 include capabilities for microbiological sampling and incubation (Fisher et al., in press).Experiments carried out in settings ranging from ridge axes (Juan de Fuca Ridge) and flanks(Mid-Atlantic Ridge, Costa Rica Rift, Juan de Fuca Ridge) to subduction zones (Cascadia,Barbados, Mariana, Nankai Trough, Central America) have provided a wealth of informationabout the driving forces for flow generated by thermal buoyancy and tectonic consolidation, therates of flow through sedimentary and igneous crustal sections, the hydrologic and elasticproperties of these sections (permeability, compressibility), and the age, composition, and rateand direction of transport of formation fluids. The original goals have been surpassed to thepoint that many new objectives have been added for recent and future installations, includingdocumenting the quantitative physics and chemistry of fluid flow within the igneous crust, andusing pressure and temperature as quantitative indicators of oceanographically, tectonically, andseismically stimulated strain, flow, chemical reaction, and microbiological nutrient supply. Inaddition, new experiments are helping to determine relations between hydrologic, tectonic,biological, and geochemical crustal systems.

This response to the ORION RFA outlines prospects for an ORION-IODP cooperativeeffort for arrays of subseafloor borehole observatories at type locations suitable for use of OOIcable or buoy infrastructure, with two primary scientific objectives: (a) hydrogeological andmicrobiological monitoring and active experiments, and (b) small-plate-scale strain monitoring.An obvious template location is the northern Juan de Fuca plate, linked to the NEPTUNE cableinfrastructure and building on an existing array of ODP/IODP CORKs. For that region, thisresponse is carefully coordinated with (and draws on text from) two allied proposals currentlyunder consideration: (a) a NEPTUNE Canada proposal for an array of Juan de Fuca boreholeobservatories as NEPTUNE node locations for our main two primary objectives, and (b) an NSF-IODP proposal for the long-term hydrological/microbiological monitoring associated with anapproved (but not yet scheduled) IODP revisit to one of those nodes, where four existing originaland multilevel CORKs currently are in operation. Below we first develop our overall scientificobjectives first in the context of the proposed NEPTUNE/Juan de Fuca array, and we also usethis array as the basis for a section detailing technical requirements. It is important to note thatthere are also several other good template borehole observatory array locations (e.g., the NankaiTrough subduction system, the MOMAR region) independent of the NEPTUNE regional cabledinfrastructure and equally suitable for developing the ORION-IODP linkage. Therefore we alsodescribe, albeit more briefly, the potential analogous efforts in these other template locationswith potential OOI buoy infrastructure or even Japanese cabled infrastructure.

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2.0 Scientific rationale for the application of a “template experiment” at Juan de Fuca Platewith NEPTUNE

The combination of access to the sub-seafloor via sealed boreholes and a cableinfrastructure in the setting offered by the northern Juan de Fuca plate provides an unprecedentedopportunity to study many fundamental questions about the dynamics of the oceanic lithosphereand the subseafloor hydrosphere. This is made evident by considering the following:1) All types of plate boundaries, divergent, convergent, and transform, are present at the marginsof this plate.2) The scale of the Juan de Fuca Plate system is ideal for studying interrelationships amongdynamic processes within the plate and along its boundaries (e.g., among episodic plate motion,internal plate strain, and earthquakes) and associated fluid flow.3) The plate is blanketed by low-permeability turbidite sediments which form a nearlycontinuous barrier to the exchange of water between the highly permeable igneous crust beneathand the ocean overhead. This confinement facilitates quantitative experiments focused on fluidflow processes within the igneous crust that would not be possible in a sediment-free setting, andallows measurements focused on plate strain to be made within the sediment section (which hasa long hydrologic drainage time constant) across the full lateral dimension of the plate from theridge to the subduction zone.4) Many years of autonomous borehole monitoring have already been completed in this andanalogous settings, and much has been learned (see CORK bibliography at end of references).The data have provided much insight into the opportunities that lie ahead (discussed next), butautonomous monitoring is severely hampered by inherent limitations on power, data storage, andtiming. Great gains will be realized in experimental lifetimes and observational fidelity throughhaving data telemetry to and power transmission from shore.5) A nearly ideal network of boreholes already exists in the northern Juan de Fuca plate region.The addition of a small number of new sites will allow a coherent view of the plate from a"hydro-tectonic" perspective, and will facilitate the first "active" subseafloor experiments in theoceanic crust (Table 1 and Fig. 1, using node-naming convention from NEPTUNE Canadaproposal).

The outline of work proposed here has been developed within the context of theseimportant considerations: tectonic (e.g., appropriate scale of plate system, all boundary typesrepresented), hydrologic (permeable crustal aquifer, low-permeability sediment cover), andtechnical (borehole access, NEPTUNE connection); it has also been developed with considerableintuitive and quantitative wisdom gained through previous experiments. For simplicity, we havesubdivided the work into two themes, fluid flow and strain monitoring. There is much overlapbetween the processes involved in each and in the observational strategy, although in some casestechnical details for the subseafloor installations may require independent holes.

2.1 Fluid flow – hydrogeological observatories on Juan de Fuca plate

Flow through oceanic crust and sediments has fundamental short- and long-termconsequences. Crustal water, warmed by regional geothermal heat flux or by the latent heat offusion of magma at seafloor spreading centers, reacts with the host formation. Flow isstimulated by the buoyancy forces created by heated crustal fluids, and by tectonic andgravitational loading. Disequilibria cause alteration of the rock matrix and mineral precipitation

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in the fractures and pores that transmit the fluids. The flow itself transports solutes and heat, andwherever flow crosses the seafloor, heat and elemental exchange between the crust and oceansresults. The volume flux of fluids across the seafloor associated with these processes is at leastas great as the annual riverine flux to the ocean. Advective heat transport constitutes a majorfraction of the total geothermal heat flow in young areas. Global chemical flux through theseafloor is significant for several ionic species, and solute-bearing water can provide a crucialsource of energy for chemosynthetic microbes both within the crust and at the seafloor.

Much has been learned about the general patterns and average rates of flow through theuppermost igneous crust and sedimentary sections in ridge crest, ridge flank, and accretionaryprism settings. However, little is known about the actual flow pathways within these sections:the depth to which igneous crustal circulation penetrates, the distribution of permeability as afunction of depth, lithology, and structure, and the degree to which some volumes of rock areisolated from, and others highly involved in, fluid transport and reaction.

Borehole experiments provide the only means to study directly these importantsubseafloor systems at more than a few meters below the seafloor. The borehole observatoryapproach was initiated in 1991 as part of the Ocean Drilling Program (ODP), with two sealedand instrumented CORK installations in the active hydrothermal "reservoir" in Middle Valley,northern Juan de Fuca Ridge. Since then, several other sites have been established through threeadditional ODP drilling expeditions in this area. All of these share common elements. First, theypenetrated only a short distance into what is inferred to be the most permeable part of theuppermost igneous crust, with the goal of defining the lateral gradients in temperature andpressure as constraints on average upper crustal permeability and rates of flow. Second, CORKexperiments were largely passive, monitoring formation and fluid response to naturalperturbations, once the disturbance due to drilling had dissipated. These efforts were highlysuccessful, but they provided only partial understanding of these complex crustal systems.While learning how crustal hydrothermal systems behave at a scale of kilometers, numerousfundamental aspects of crustal circulation remained unconstrained. In 2004 as part of the firstexpedition of the Integrated Ocean Drilling Program (IODP), a new effort was begun to establisha three-dimensional matrix of monitoring points in the crust; this effort is expected to continuewith an approved but still unscheduled revisit of the US non-riser IODP drilling vessel to thearea. The boreholes and CORKs comprising this network include deeper penetration of the crust,multi-level monitoring to study the fluid and microbiological compartmentalization, and theinitiation of active cross-hole experiments in the crust (Fig. 2). This network of boreholes is to beused in the first controlled cross-hole, crustal-scale hydrogeologic experiments in oceanic crust.Similar tests have been conducted in aquifers and reservoirs for decades on land, but never in thedeep sea. These tests will be profoundly different from other (passive) experiments that havebeen completed previously on the eastern flank of the Juan de Fuca Ridge. Another detailedstudy is planned as a follow-on to initial IODP borehole experiments in the Cascadiaaccretionary prism currently scheduled to begin in 2005. Both of these efforts will involveequipment that will benefit greatly from the power and interactive experimental control that willbe provided by NEPTUNE. Examples described in more detail in section 4 below includepumps, flow meters, and samplers for long-term controlled hydrologic and biogeochemicalperturbation tests, controllable valves for natural production tests, conservative-element injectorsfor tracer tests, analysers for fluid-composition monitoring, and in-situ microbiological samplersand incubation systems.

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In addition to the ideal setting for borehole experiments, the Juan de Fuca plate providesanother unique opportunity for studying crustal hydrogeology. In several locations volcanicseamounts created near the ridge axis are sufficiently elevated to have avoided complete burialby the flat-lying turbidite sediments of Cascadia Basin. The resulting outcrops constitute"permeable penetrators" that provide localized routes for fluid exchange between the upperigneous crust and the ocean. Observations indicate that most are sufficiently small to be keptwarm by hydrothermal circulation, and only discharge occurs, although outcrops larger than acritical size appear to become advectively cooled to the point that the negative buoyancy causesthem to serve as regional recharge points. Two such penetrators lie near borehole sites, and willbe the focus of seafloor experiments to constrain the average flow through them and to allownatural variability of flow (e.g., tidally or tectonically mediated) to be documented. "Baby Bare"(Fig. 3; Table 1; named for its small size and lack of sediment cover) is located a few km southof the H-5 borehole network shown in Fig. 2 and can be serviced by a cable access point at thoseboreholes. Similarly, "Zona Bare" lies a few km south of the H-6 boreholes and can be servicedby that access point. Both sub-seafloor and water column instruments (mini-boreholes, seepmeters, thermal and chemical sensors) will be deployed to constrain seafloor fluid, heat, andchemical flow and the influence on seafloor mineralization and biological communities, and onbenthic seawater chemistry, thermal structure, and biology. The relative rarity of basementoutcrops in the work area of this proposal helps with interpretation of thermal, chemical, andmicrobiological data, but these features are extremely common on a global basis. As many as80,000-100,000 seamounts (as well as numerous large igneous provinces and fracture zones)provide high-permeability pathways for crustal fluids to be exchanged with the overlying ocean.Studies in several settings have shown that crustal fluids may travel distances of tens or hundredsof kilometers between outcrops. The combination of closely spaced borehole observatories andobservations on outcrops on the Juan de Fuca plate provides a unique opportunity to understandthe dynamics and far-reaching impacts of this circulation.

Sites where detailed borehole and outcrop hydrogeology experiments will be carried outare summarized in Figure 1 and Table 1. These include the sites described above, as well asboreholes where super-hydrostatic conditions (and thus potential for natural production) areknown to occur (H-1, Site 858, and H-3, ODP Site 1025).

2.2 Strain monitoring observatories on the Juan de Fuca Plate

The second scientific thrust of this proposal dovetails with efforts proposed byseismology, geodetics, tsunami, physical oceanography, ridge-crest, and hydrates NEPTUNECanada groups, as well as the hydrologic studies outlined above. It involves a plate-widenetwork of boreholes, extending from the ridge axis to the subduction zone accretionary prism(Fig. 1), designed to document both large-scale hydrologic processes in the upper oceanic crustand regional-scale plate motion and strain. As articulated in the introduction, the Juan de Fucaregion lends itself to this experiment because of the dimensions of the plate and its extensivesediment cover. The combination of these factors with borehole access to the subseafloor andthe NEPTUNE infrastructure completes a unique equation. Without each of the elements, theexperiment would simply not be possible: The number of sites required to document coherentsignals associated with motion within the plate and along its boundaries is too great for thenetwork to be serviced by manned or robotic submersibles, and reaching into the seismic

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frequency band places demands on power, data storage, and timing accuracy that are too greatfor autonomous instruments. NEPTUNE connection is essential.

Hydrologic response to tectonic and seismic events has been observed in severalinstances in the past; some examples from the Juan de Fuca region and elsewhere are shown inFig. 4 to provide the reader with a sense of what is proposed here. These include hydrologic(formation pressure) response to teleseismic surface waves (Fig. 4a), the near- and far-field strainassociated with episodic seafloor spreading and related earthquake swarms (Figs. 4b and 4c,respectively), a propagating aseismic subduction zone slip event (Fig. 4d), and secular inter-earthquake strain accumulating at a subduction zone (Fig. 4e). These examples (and numerousothers like them) clearly demonstrate several things:1) Plate strain events occur often enough to make their study feasible in the course of a few-yearto few-decade monitoring epoch.2) Formation-fluid pressure provides a sensitive and quantitative proxy for volumetric strain.Using pressure as an intermediary between matrix strain and sensor allows observations that aremuch less sensitive to heterogeneities than measurements made with directional strain gaugescoupled directly to the local rock matrix. Quantitative calibration between pressure and strain isprovided by the local pressure response to seafloor tidal loading, and the sensitivity is very good:a typical strain response is roughly 0.3 x 10-6/kPa; this coupled with instrumental resolution ofbetter than 1 Pa would provide an detection threshold of 10-9 in the absence of environmentalnoise.3) Plate boundary slip events produce intra-plate strain of the order of 10-6 over distances ofhundreds of km, and correspondingly easily resolved pressure signals.4) Surprises can be expected. With monitoring carried out to date, a variety of events have beenseen that could have been documented in no other way, and they beg new basic geodynamicalquestions. For example, the slip event witnessed in the outer Nankai accretionary prism (Fig. 4d)occurred with no resolvable local seismicity. The pressure pulse is interpreted to result from theseaward tail of a migrating dislocation along the subduction plate boundary. Whether thisprocess relieves or adds stress along the seismogenic part of the thrust boundary is not known.Another surprise is exemplified by the plate deformation reflected in the transient shown in Fig.4c which is much larger than that which would be associated with the accompanying earthquakeson the adjacent ridge axis. It appears that a large proportion of the energy of this seafloorspreading event was aseismic. The question is raised whether the earthquakes of this and otherswarms are in fact simply small seismic expressions of sub-seismic slip events. In addition tothese pressure perturbations, temperature perturbations have also been observed at remotelocations, indicating that there can be hydrogeologic communication across vast distances withinthe oceanic crust, tens to hundreds of kilometers, an inference consistent with thermal andchemical observations near the seafloor, and with observations of seismic-hydrologic linkages oncontinental crust. The same properties that make the deep ocean environment "quiet" enough todetect small seismic and tectonic events also allow high resolution in hydrogeologic experimentsacross these vast distances.

The presence of these and other signals provides great motivation for the study proposedhere, and leads to a strategy that would allow steady and episodic plate and plate-boundary strainto be documented properly. We have learned that many of these signals are a combination oftectonic and hydrologic components. Separating them is often impossible in the formationswhere the holes are terminated, especially in cases where time-dependent strain signals (e.g.,viscoelastic deformation) may have characteristic time constants that are similar to those of the

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related hydrologic processes (e.g., drainage). To avoid this problem and to allow strain to becharacterized from high to very low frequencies (seismic to secular), a new strategy has beenproposed. This will involve completing monitoring horizons hydrologically mid-way betweenthe upper seafloor and lower permeable basement interfaces. These, combined with thebasement intervals already completed at many of the sites, will allow for truly broad-bandmonitoring that will address both geodynamic and hydrologic objectives.

2.3 The proposed network of Juan de Fuca borehole observatoriesThe network proposed (Fig. 1) builds on a suite of holes already completed, with many

individual sites sharing objectives with other programs to be implemented through NEPTUNE(Table 1). The network extends from the ridge-axis, to "mid-plate" locations (we qualify the"mid-plate sites" with quotation marks because we know that even there, plate motion is notprecisely steady as it might be thousands of km from any boundaries), and on across thesubduction plate boundary, with site spacing compressed towards each plate boundary wherehydrologic and episodic strain gradients are bound to be greatest. From a geodynamics point ofview, the rationale for the distribution can be most easily described by considering the following"quantum-plate-motion" scenario and the way that "motion quanta" can be observed with thisnetwork and other complementary NEPTUNE monitoring sites. The basis for this scenario is amodel for internal plate motion that involves frequent pulses of motion at different segments ofthe plate's boundaries. The pulses may have a huge range of magnitudes and may be seismic oraseismic. The scenario might follow a sequence like this:

1) Motion occurs at the Juan de Fuca Ridge axis, Cascadia subduction zone, or Nootkatransform fault. This might be observed indirectly (by way of plate-boundary seismicity), ordirectly and quantitatively (e.g., via horizontal acoustic ranging across the Endeavour or MiddleValley rifts and/or changes in depth of bottom pressure recorders at the ridge axis or theCascadia continental margin).2) Elastic strain is transmitted "instantaneously" (at seismic velocity) to all borehole monitoringsites and is observed via increases or decreases in formation fluid pressure in regions ofextension and contraction, respectively.3) Elastic strain is followed by visco-elastic strain which propagates across the plate at a ratethat can be documented in the hydrologically confined sedimentary monitoring intervals. Therate will provide constraints on bulk elastic properties of the plate and on the viscous couplingbetween the plate and asthenosphere.4) In the case of slow-slip events (e.g., on the subduction thrust, as has been detected butincompletely characterized off Southwestern Japan), slip can be witnessed directly by theborehole network. The rate of subseismic motion will provide important constraints on thetsunamigenic potential for faults that pass through major changes in lithology.5) Strain will have a direct effect on pore volume, permeability, and formation fluid flow as wellas pressure. These and other consequences can be observed via changes in electrical properties,formation compliance, seafloor fluid flux, formation- and vent-fluid temperatures andcompositions, and possibly even microbiological productivity. Coordinated observations of allof these will be made possible with NEPTUNE.6) With suitable improvements in detection threshold of acoustic ranging methods, episodicstrain events may be detected by geodetic NEPTUNE monitoring sites that are linkedcontinuously or in campaign mode to GPS navigation.

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7) Between "quantum events", secular accumulation of strain can be monitored within the plateand near the plate boundaries, and "steady" plate motion can be observed via GPS-linkedgeodetic sites.8) Throughout cycles of boundary slip and plate deformation, strain that is monitored within thesedimentary monitoring intervals can be compared with co-variations in the rate and nature ofseismicity observed with the NEPTUNE seismic instrument network that occur below currentdetection limits.

To document such processes quantitatively and with confidence requires a network ofsites that spans the full dimensions of the plate, and has observation points that are closelyenough spaced to allow an unaliased view of the associated seismic, hydrologic, and geodynamicsignals. The network proposed constitutes one we consider to be an effective, but an essentialminimum to provide this view, and one that will provide continuous data that are highlycomplementary to others collected in the NEPTUNE system.

A similar scenario can be articulated for hydrologic processes that are not tectonic inorigin but that may nevertheless be coherent over scales of hundreds of km. Thermal andgeochemical observations demonstrate that such large-scale interconnections are present overmany tens of km, and it is a reasonable inference that hydrologic communication does take placeover the full scale of this plate, from the subduction zone to near the ridge axis. The samenetwork of sites linking outcrops and boreholes that penetrate the igneous crust will allow suchlarge-scale intercommunication to be confirmed and quantified. In this way, site-specificobjectives (such as those at H-1, H-5, and H-8) can be met at the same time that the entire plateis watched in a coherent fashion. This whole-plate approach represents arguably the best waythe NEPTUNE infrastructure can be utilized.

2.4 Microbiological investigations

Multiple lines of evidence suggest that microbial activity within the huge volume ofoceanic basement may comprise a sizeable biomass and harbor consortia of microorganisms withpotentially novel characteristics (e.g., Gold 1992; Baross et al. 1994; Fisk et al. 1998; Torsvik et al.1998; Furnes et al. 2001; Thorseth et al. 2001; Cowen et al. 2003a). The oceanic basement offersgreat potential for microbial growth and subsequent geomicrobial control of large geochemicalfluxes associated with seafloor hydrothermal systems. In essence, the ocean basement may actas a giant bioreactor, mediating water-rock exchanges and buffering the chemical composition ofbasement fluids and ultimately of seawater. Evidence of microbial activity within basement rockcores include bioelement distributions, morphological indications of cells, etch marks in freshglass, precipitation of alteration products enriched in Fe and Mn, evident DNA staining withfluorescent dyes, selective staining by fluorescently labeled probes specific for archaeal andbacterial 16S-ribosomal RNA, and stable carbon isotopic values consistent with fractionationduring microbial activity (Fisk et al. 1998; Furnes et al. 2001; Thorseth et al. 2001). RibosomalRNA gene sequencing analyses of basement fluids sampled directly from the discharge spigot atthe top of the overpressured borehole 1026B indicated a potentially complex basement ecology(Cowen et al. 2003).

The proposed plate-scale cabled network will advance our ability to exploit theunprecedented opportunities already provided by long-term IODP borehole-CORK observatoriesfor geochemical, microbiological and ecological characterization of basement ecosystems. Muchcan be learned about a community by their response to changes. For example, pulsed fluid flow

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could control sloughing and transport rates of cells and other material from channel surfaces,fluid refresh rates past attached microorganisms, fluid chemistry due to fluctuations inhydrologic plumbing and/or flow rates or in exchange rates across the sediment-basementinterface. Real-time transmission of data and commands, provided by the proposed cabledobservatory, will enable the remote control of data and physical sample collection rates inimmediate response to perturbations in seismic, temperature, pressure, or other sensor signals.Perturbations range from the effects of tidal-scale fluctuations in fluid flow (Davis and Becker,1999) to the effects of intermittent tectonic or magmatic events. Recent evidence suggests thatearthquake activity can influence hydrologic processes at sites quite distant from the earthquakecenters, although the response can be delayed days to weeks (Johnson et al. 2000; Bohnenstiehlet al. 2002; Lilley et al. 2003; Davis et al. 2004). Directed modification of instrument samplingrates in anticipation of a potential local response to a significant distant perturbation, wouldgreatly increase the chances of sampling critical early phases of any microbial or geochemicalresponse. The proposed time-series instruments and samplers will support studies of microbialgenetic and metabolic diversity and community metabolic activity in close conjunction withgeochemical measurements (e.g., redox conditions). Instrument interfaces will be designed toaccommodate additional sensors, analyzers, or sampler/incubators as they become available.

3.0 Technical description of proposed installations

All of the boreholes in the NEPTUNE/Juan de Fuca array conceptually described abovewould be completed with various types of CORKs (circulation obviation retrofit kits), the basicmeans by which holes can be sealed and instrumented for long-term "legacy" use. Since the firstCORK installations in 1991, many improvements have been made to allow greater ease of useand a broader range of applications. Installations can now be completed that are relativelyinexpensive at one end of the complexity scale (Fig. 5a), and that provide access to multipleformation levels at the other (Fig. 5b). There are currently three main types of CORKinstallations, the CORK and Advanced CORK shown in Fig. 5, and the multi-level CORK-IIillustrated in Fig. 6 and described in further detail below. In addition, there are currentlyproposals under evaluation for development for three different variants or new applications forCORKs, of which two would be parts of the proposed array: simple, so-called “primitive” or P-CORKs for single interval monitoring of formation pressures in deeper sediments as proxy forplate strain, and so-called “SeisCORKs” incorporating 1-100 Hz seismic monitoring potentiallyat different levels within the same hole. These are described in further detail below.

3.1 CORK-II Instrumentation

Three multilevel CORK-II systems were deployed on the Juan de Fuca plate during thefirst IODP expedition, and three more are planned for the approved follow-on drillingexpedition. As described in the NSF-IODP proposal for the instrumentation and engineering forthe three installations still to be made, each system will include the following components (Fig.6): (1) a well-head/instrument hanger to seal the uppermost casing and houses data loggers,submersible underwater-mateable connectors, pressure gauges, terminations and valving for fluidlines running from formation, and OsmoSamplers; (2) 4-1/2” liner casing suspended below theinstrument hanger; (3) one or more casing packers incorporated within the liner casing; (4)hydraulic lines outside the liner casing from isolated zones to wellhead, including pressure, fluid

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sampling, and microbiology (1/2") lines that terminate in small screens in the isolated intervals;(5) a seat for a wireline-retrievable plug near the bottom of the liner (bottom plug), from whichvarious samplers and instruments will be hung; and (6) a seat for an top plug that hangs in thewellhead, suspending a sensor string within the liner. The new installations will monitor twogeological intervals in Hole 1027C, three in Hole SR-2A, and one in Hole SR-2B, and provide acapability for periodically checking pressure with fully-cased intervals in all three holes.

When the next drilling expedition is scheduled, costs for cones, casing, umbilicals, and

other CORK hardware will be included in the program budget for the US non-riser ship operator.

Costs for instrumentation that will hang on or below the CORKs are included in an NSF-IODP

proposal currently under evaluation. Also included in that proposal are the costs for qualified

consulting engineers to oversee an extensive set of engineering design and development tasks

well in advance of the actual installations.Proposed instrumentation in the CORK systems includes pressure monitoring of each

sealed interval, autonomous long-term temperature loggers suspended in the sealed hole,autonomous fluid “OsmoSamplers” suspended in the sealed hole and independentOsmoSamplers attached to valves on the wellhead, and autonomous microbiological samplersboth downhole and at the wellhead valves. Pressure monitoring in all multi-level CORKs isaccomplished by a data logger and wellhead gauges that are connected to the isolated intervalsvia incompliant tubing umbilicals. Earlier generations of CORK systems used pressure gaugesand data loggers capable of measuring absolute pressure with resolution of a few kPa and storingseveral megabytes (Mb) of data typically recorded at sampling rates of 10 minutes to an hour.More recent pressure packages have significantly better pressure resolution and temperaturestability, and larger memories allowing for more frequent sampling at high resolution. Weimagine it would be fairly straightforward to adapt and link the pressure logging systems to OOIinfrastructure, with modest power and bandwidth requirements.

On the other hand, the multi-level CORK-II’s sensor strings incorporate long-termdownhole autonomous temperature loggers available from two commercial manufacturers (OnsetComputer and Antares DataSystem), as well as autonomous downhole fluid and microbiologicalOsmoSamplers; these all require physical recovery after years of deployment to access data andsamples. Two kinds of fluid sampler packages have been deployed and are planned for the newinstallations: (1) “downhole” samplers hung below the bottom plug within 4-1/2” casing, and (2)“seafloor” samplers attached at the wellhead and connected to small-bore lines and screens formonitoring the composition of fluids at depth. The seafloor samplers require periodic servicingwith submersibles, ideally on an annual or biannual basis. The downhole packages are typicallysuspended on Spectra line and consist of 3-6 OsmoSamplers, one or more self-containedtemperature loggers, microbiological colonization systems, and a sinker bar. Typically, each ofthe downhole packages is capable of running for 2-5 years, but physical recovery of the string isrequired for access to data and samples.

The opportunities for real-time data offered by linking to OOI infrastructure will providegreat incentive to take the next technological step to engineer downhole signal conditioning andtransmission uphole and to shore. In fact, original CORKs typically included thermistor cablesconnected to a data logger that recorded both temperatures and pressures. With ORION support,we would propose to engineer an analogous sensor string, but more advanced in incorporatingdownhole signal conditioning and transmission via OOI protocols. That this is feasible (at leastat low to moderate temperatures) is demonstrated by an early CORK sensor string withdownhole signal conditioning and serial communication from multiple temperature and pressure

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sensors to a seafloor data logger (Foucher et al., 1997). For downhole fluid/microbiologicalsampling, we would propose ORION support for adding an electronic analysis capability to thebasic OsmoSampler design, again with signal conditioning for transmission uphole and to shorevia OOI protocols. This may be more challenging than for downhole temperatures, and wewould also request consulting engineering support to design a system that both accommodatesdownhole signal conditioning and preserves the current option for autonomous samplers withperiodic recovery and replacement.

3.2 “P-CORK” concept (as described in IODP pre-proposal 655-Pre)

The best method for completing holes for plate-strain monitoring will depend on a varietyof factors (e.g., whether there is a need at some sites to provide for other instrumentation such asbroad-band seismometers that would require open-hole access and a large-diameter casing). Thesimplest, cheapest, and quickest technique would involve “primitive” CORKs made up withdecommissioned drill collars and pipe that would be drilled in a single pipe trip. These wouldinclude an expendable bit, a bottom-hole assembly that would provide a permeable access to theformation, an upper seal and data logger system, and a supra-seafloor release joint. This wouldbe a functional equivalent to the original single-interval CORK (Fig. 5a) but without thecomplexities and costs (monetary and time) associated with a reentry cone and casing. Thisconfiguration would yield an internal hole diameter of ~4” and allow later access, but only byremoving the sensor/logger package and disrupting the monitoring. If hole access is a priority atany given site, then a completion similar to an ACORK would be called for. This could beaccomplished by coring, which may be advantageous at some sites for scientific and safetyreasons.

As noted above, all CORK designs to date utilize seafloor data loggers and gauges, andthe same would be true for the P-CORK. Thus, the P-CORK would have the same potential forstraightforward modification for linkage to OOI infrastructure.

3.3 Seismometers on CORKs (SeisCORKs)

The purpose of SeisCORKs is to simultaneously acquire borehole seismic data and

hydrogeological and biogeochemical data using a single CORK system (Stephen, Pettigrew et al.

2004) (Fig. 7). The merits of SeisCORKs fall into two categories: 1) In a passive recording

mode, seismometers on CORKs will enable the simultaneous and co-located acquisition of nano-

and micro-earthquake activity with hydrogeological and biogeochemical measurements for an

improved understanding of sub-seafloor processes. Biogeochemical and hydrogeological events

may be associated (possibly as precursors) with earthquakes. It may also be possible to detect

micro-earthquake activity associated with long-term pumping and flow experiments as the

thermal and pressure regime around the borehole changes. The location of the earthquakes can

be used as a proxy for a map of fluid flow. (This is similar to using micro-earthquake activity to

monitor fluid flow in petroleum reservoirs.) 2) In an active recording mode, seismometers on

CORKS will facilitate the simultaneous acquisition of offset-VSP and OBS refraction survey

data to measure the lateral heterogeneity and anisotropy of the upper ocean crust which are

proxies for porosity variations and fracture orientation respectively. The structure of upper

oceanic crust provides the framework in which the hydrogeology processes take place.

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SeisCORKs can be used in the future for a broad range of borehole geophysical

experiments targeted at various geological and seismic processes, however the scientific focus

initially will be the Juan de Fuca Hydrogeology program. Determination of relations between

hydrogeologic and seismic anisotropy in the upper crust was a goal of IODP Leg 301 and will

continue to be a goal of the follow-up expedition. Adding long-term seismometers should help to

achieve this goal and also to assess lateral heterogeneity in crustal properties around the CORK

sites. We feel that this will best be accomplished by a combined OBS (ocean bottom

seismometer) refraction and offset-VSP (vertical seismic profile) experiment. Given the

logistical difficulties of coordinating the operations schedules of two vessels on the high seas, the

best approach for the combined seismic experiment is to integrate the VLF (1-100Hz) borehole

geophones with one of the CORKs that will be installed in the follow-up expedition.

Borehole seismic acquisition systems in the frequency band 1-100Hz are commercially

available; however, they are designed to be installed and operated on land with essentially

unlimited power and data storage and with reliable data telemetry. In a SeisCORK system

modifications will be necessary to install the borehole equipment with the traditional CORK

systems either from the drill ship or from a conventional research vessel (using a Control Vehicle

or ROV). There are also hybrid designs where the basic CORK is installed from the drill ship

but a slim sensor string could be installed later by ROV.

3.4 Wellhead (CORK platform) microbial geochemical sampling

Fluids discharged from sampling ports at the top of the over-pressured ODP borehole1026B, on the flanks of the Juan de Fuca Ridge (JFR), provide a unique opportunity to obtainlarge volumes of basement fluids for a variety of analyses and experiments addressing themicrobial communities of aging ocean basement (Cowen et al. 2003). However, the older CORKinstallation at 1026B suffered from the cumulative contamination of the ascending fluids fromchemical and biological processes associated with bare iron borehole liner and casing, andpossible infiltration of sediment pore waters through any joint leaks. The new generationmicrobiological Fluid Delivery Systems (FDSs) associated with the new (July/August 2004)CORK installations at JFR flank sites should substantially overcome these concerns. The newFDS was specifically designed to minimize chemical contamination and surface biofouling; theyemploy a dedicated biological sampling line consisting of inert PVDF tubing extending from thefluid intake ports at the bottom of the borehole all the way to the sampling spigot at the CORK’sseafloor platform; unreactive titanium connectors have replaced steel connectors. The boreholeliner adjacent to the FDS fluid intake at depth is covered in a double layer of heavy gauge shrink-wrap Teflon. The new FDSs will thus provide reliable seafloor observatory windows to thebasement biosphere. The microbial geochemical (MGC) component of the proposal emphasizesthe new FDS installations to study the basement microbial community structure and activity in thecontext of basement geochemical and physical conditions (e.g., inorganic and organic chemistry,temperature, redox condition).

Each CORK observatory intended for MGC observations will be instrumented using anopen architecture which allows for different or additional instruments/sensors to be added at anytime. An MGC sampling manifold will provide the interface between the CORK’s seafloor fluiddelivery connector/valve and the instrumented sled. The manifold is equipped with multiplesampling/instrument insertion ports and robust servo-operated valves. The primary instrument

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sled will carry a selection of analyzers, sensors, and samplers to the CORK platform. Theinstrument sled will be “plugged” into the MGB Sampling Manifold in terms of both access tothe basement fluid flow and to power/command the manifold servo-valves. Instrument samplingintervals, rates, and volumes will be controllable via cabled observatory infrastructure.

A filtration/pump system (modified McLane’s Water Transfer System) will permit in situfiltration of small to large volumes of fluid past assorted filters which are subsequently fixed(poisoned or extracted) in situ to stop further metabolic/enzymatic activity. A wide variety offilters, post-filtration extraction columns and whole fluid samplers can be incorporated into thetime-series filtration system. Temperature controlled incubation chambers will be added underseparate funding. Geochemical measurements will include an In Situ Electrochemical(voltammetry) Analyzer (ISEA), providing real-time, simultaneous measurements of O2, H2O2,HS-, S(0), Sx

2-, S2O3, S4O6, Fe(II), Fe(III), FeS(aq), Mn(II), and Zn(II), key redox-sensitiveconstituents (Luther III et al. 2001) that reflect the past biogeochemical history and present redox(metabolic) conditions of the basement fluids. Multiple (redundant) electrodes are in line withthe flow to the filtration system providing precise correspondence between sample collection andkey redox measurements. The on-site voltammetric analyzer minimizes noise and attenuation ofthe electrochemical signal. The prototype instrument sled (including the ISEA, the waterfiltration system, temperature probes, and flow rate) will be field-tested at one of the proposedCORK observatories in September, 2005.

4.0 Other template locations accessible with OOI buoy infrastructure

The bulk of this proposal focuses on the Juan de Fuca/NEPTUNE region as the templatefor description of the proposed ORION-IODP borehole monitoring efforts; this is where theconcepts are best developed owing to the history of ODP/IODP CORK observatories there andyears of NEPTUNE planning efforts to date. It cannot be overemphasized that the concepts areequally valid for other well-studied regions of the seafloor outside of the NEPTUNE regionalcabled observatory but accessible with OOI buoy infrastructure. There at least two excellentexamples of small-plate-scale locations where comparable scientific investigations to thosedescribed above are also justified by surveys and existing ODP borehole observatories: theNankai Trough/Shikoku basin area that will be a prime focus of IODP “NanTroSEIZE” drilling,and the section of the Cocos plate that incorporates the Costa Rica Rift and Costa Rica Trench.In addition, the hydrogeological/microbiological aspect of the proposed work could easily applyto focal areas of ridge-crest studies that may include a significant IODP drilling contribution,e.g., the RIDGE2000 Intensive Studies Site at the East Pacific Rise, and the MOMAR(Monitoring the Mid-Atlantic Ridge) initiative in the North Atlantic.

In the Nankai Trough/Shikoku Basin area, pressures from Advanced CORKs installed byODP in 2001 show signals from seismic and aseismic deformation at the subduction plateboundary (Davis et al., in review); this is another excellent location for a small-plate-scale strain-monitoring experiment utilizing a spatial array of borehole observatories. Elements of such anarray could be incorporated within the high-priority IODP Nankai Trough Seismogenic ZoneExperiments (NanTroSEIZE), which has a borehole observatory focus on understanding therelationship among fluid pressures and flow, tectonic forces, and the earthquake cycle. Thus, acombined hydrogeological/strain-monitoring experiment on cabled or buoy infrastructure similarto that described above at the Juan de Fuca plate could be equally fruitful. With the location nearJapan, international collaboration is certainly called for, and there may even be opportunities for

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sharing infrastructure costs, particularly if Japan invests in offshore cable and/or buoyobservatory infrastructure.

5.0 Compilation of Efforts Being Proposed for ORION-IODP Support

The work described above is intended as a cooperative IODP-ORION project, withshared support. In attempting to distinguish how the proposed support might be allocatedbetween the two programs, it is important to understand the funding paradigm for CORKsestablished during ODP, and to realize that a significant aspect of this model probably willchange during IODP. During ODP, the drilling program provided from commingled programfunds the seafloor and subseafloor infrastructure (casing, reentry cone, CORK body) andnecessary engineering support for each CORK; the proponents sought NSF-ODP researchfunding for the long-term instrumentation hung in the CORK and the post-installation supportfor submersible revisits and servicing. During IODP, the drilling operators probably cannotprovide all the necessary engineering support for the increasingly sophisticated installations, soproviding support for much of that critical aspect may be shifting to the NSF-IODP researchfunding requests. This is the case for the NSF proposal for the instrumentation associated withthe approved but not yet scheduled IODP revisit to the area mentioned above.

For the proposed ORION-IODP cooperative effort, it is not fully clear how fundingwould be coordinated. Building on the ODP model, one obvious possibility would be for IODPto provide the seafloor/subseafloor infrastructure from commingled IODP funds, IODPscientists/proponents to seek NSF-IODP research funding for the in-hole instrumentation andengineering required to use that instrumentation in the holes, and for ORION support to berequested for the engineering and material costs of adapting and linking the instrumentation tothe OOI infrastructure (NEPTUNE cable or OOI buoys). It is also not fully clear whether OOIoperators would be able to support all the necessary engineering effort to adapt and link CORKinstrumentation to the OOI infrastructure.

In section 3 we described most of the required elements for the Juan de Fuca templatelocation, for the sake of the main stated objective of the ORION RFA – to assure that the OOIinfrastructure will be designed to accommodate all needs of high priority ORION observatoryscience. In the remainder of this section, we consolidate a listing of the efforts for which, subjectto guidance from program managers, we might reasonably propose partial or full support fromORION research funds and/or OOI infrastructure operator support.

• Consulting engineering to ensure physical compatibility with basic ODP/IODPoperational constraints and electronic compatibility with OOI operational constraints

• Physical link-ups (“extension cables”) from boreholes to OOI nodes (NEPTUNE cablenodes or OOI buoy nodes)

• Design and construction of OOI-compatible communications system for pressure dataloggers

• Design and construction of downhole temperature strings with signal conditioning andcommunication via OOI protocols

• Design and construction of downhole fluid and microbiological analyzers compatiblewith OsmoSamplers and OOI communication protocols

• Design and construction of SeisCORK 1-100 Hz downhole monitoring and seafloorrecording system compatible with OOI communication protocols

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• Design and construction of wellhead fluid/microbiological sampling system compatiblewith OOI communication protocols

6.0 Program and Data Management

As a joint IODP-ORION project, our proposed borehole observatory array(s) would besubject to the program and data management policies and procedures of both IODP and ORION.We expect that the two programs will have reasonably consistent policies. There are multipleaspects to these management issues, some of which are being addressed already. These include,among others:

Choosing borehole site locations. Juan de Fuca plate locations (all in Canadian waters) arealready proposed to NEPTUNE Canada, as described above.

Allocation of IODP drillship time. Juan de Fuca hydrogeology locations are alreadyinstrumented or approved for a near-future IODP expedition. Additional strain monitoring sitesand development of the “P-CORK” are described in an IODP pre-proposal, and a full IODPdrilling proposal has been invited by the IODP Science Steering and Evaluation Panel. PotentialNankai Trough seismogenesis locations are already instrumented (Muroto Transect) or approvedfor multiple IODP expeditions when the new non-riser and/or riser drillships begin operations.

Funding for instrumentation and submersible support. NSF-OCE-ODP is currentlysupporting a five-year program (OCE-0400471, Becker, Davis, Wheat, Jannasch, co-PI’s) at thethree multi-level CORKs installed during IODP Expedition 301 and four original CORKsinstalled during ODP. NSF-OCE-IODP is currently evaluating a second five-year proposal(Fisher, Becker, Clark, Cowen, Davis, Wheat, Jannasch, co-PI’s) for instrumentation, cross-holetracer testing, and submersible support for the additional approved multi-level installations.NSF-OCE-ODP also has recently supported an SGER grant for an engineering feasibility studyfor SeisCORKs (Stephen, PI). This response to the ORION RFA outlines additional efforts thatwould be required for the proposed borehole observatory arrays linked to the OOI infrastructure,with a combination of support to be sought from NSF-IODP and NSF-ORION programs.

Access to observatory boreholes. For ODP borehole observatories, the groups of PI’s wererelatively small, and any questions regarding access were generally handled by discussion amongPI’s. As IODP borehole observatories and ORION/OOI observatories become moresophisticated and multi-disciplinary, the potential for incompatibilities among users orexperiments increases, and the need for a clear coordinating authority becomes greater. Asdescribed above, our proposed well-head micro-geochemical sampling system will have an openarchitecture that should allow multiple users. The central management organization for IODP,IODP Management International, is in process of setting up a task force that will deal withquestions of access to borehole observatories, among other issues. Likewise, we expect theORION management and/or advisory structure to set policies for access to OOI infrastructure.For this joint project, and other potential IODP-ORION programs, it might be appropriate toform some sort of joint ORION-IODP body or at least ask the two policy-making bodies toformulate a joint policy.

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Data access and archiving. IODP has a well-developed data access policy, although theapplication to borehole observatories needs further development by the task force currently beingformed. The IODP policy is for open access to all IODP data, after a proprietary period of a yearfor the original investigators, and IODP also will provide a program-wide data archivingcapability. Similarly, we understand that ORION will have an open access data policy, withsystem-wide archiving, with a potential proprietary period for original investigators. Thus, wewould expect that the data from our proposed borehole observatories would become openlyavailable after a nominal proprietary period. There are details to be worked out between theIODP and ORION programs in defining how to apply a proprietary period for a continuousstream of data, and how to share any data-archiving responsibilities, but we expect these can beworked out jointly.

Sample access and archiving. The fluid and microbiological samples that may be producedfrom some borehole observatories may be limited in quantity and have many ephemeralproperties. Thus, it may be more difficult to define an “open” sample access and archivingpolicy for these samples than for the observatory data stream. We expect that this issue mayarise for many kinds of OOI/ORION ocean observatories, and it is also among the issues to beconsidered by the IODP borehole observatory task force. We also would expect to follow anyjointly developed policy.

7.0 Ship and Submersible Needs

CORKs to date have typically been installed during an ODP or IODP drilling expedition,and we would expect the same for future installations, with scheduling handled by the IODPdrilling proposal structure and the IODP central management organization. CORKs have alsotypically required servicing via manned or unmanned submersible at regular periods, optimallyannually or biannually. To date, the NSF-ODP office has supported the bulk of the necessarysubmersible time. If our proposal is accepted as a joint ORION-IODP effort, then sharedfunding of the necessary submersible time might be appropriate. There would be an initialinvestment in terms of actually making the linkage to the OOI infrastructure, but thereafter, thereal-time communications and power capabilities of the OOI infrastructure should result in areduced requirement for submersible support. As an initial estimate, the fully developedNEPTUNE array of borehole observatories would probably require an initial investment ofsubmersible time on the order of three weeks per year.

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Figure 1. Ocean crustal hydrogeology borehole and permeable-outcrop monitoring sites (seeTable 1 for details).

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Figure 2. Detailed map of hydrogeology Site H-5. Borehole locations are shown in context ofbasement topography which is buried by flat-lying sediments (stripped away) ranging inthickness from roughly 250 m along the basement ridge to 700 m above the valley. Anexception occurs roughly 6 km to the south of Holes 1301A and B (south of this map area) at thesediment-free "Baby Bare" seamount which rises 80 m above the sediment surface (see Fig. 3).Passive monitoring and active hydrologic experiments are planned for each of the borehole sitesand the basement outcrop.

Figure 3. Seismic sectionthrough and seafloor heat-flux profile across BabyBare seamount atNEPTUNE hydrogeologysite H-5. The degree towhich estimated isothermsfollow the sediment-basment interface indicatesthe degree to whichbasement is kept warm byfluid circulating within anddischarging through thispermeable outcrop (50, 60,and 70 oC contours arecalculated from the heatflux).

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Figure 4 a-e. Formation pressures measured in boreholes that penetrate sediments and buriedigneous crust in ridge-crest, ridge-flank, and subduction-zone settings.

Figure 4a. Teleseismic surface waves generated by a Mw 7.4 earthquake beneath Oaxaca,Mexico, observed as ground motion by a broadband seismometer, and as bottom-water andformation fluid pressure in a borehole on the Juan de Fuca Ridge flank at roughly the sameepicentral range. High-frequency NEPTUNE monitoring will provide unaliased characterizationof the conversion of surface waves to pressure, and a proper determination of the amplitude offormation pressure variations relative to bottom water pressure variations and ground motion(with the latter constrained by co-located NEPTUNE seismometers).

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Figure 4b. Pressure changes recorded in Hole 857D at the time of a seafloor spreading event inMiddle Valley, northern Juan de Fuca Ridge. The initial pressure drop occurred in discrete stepsat times of the large earthquakes; the signs are consistent with the location of the site relative tothe location of the earthquakes and the direction of motion indicated by moment tensor solutions.The maximum pressure anomaly occurred nearly two weeks after the swarm as a consequence ofhydraulic diffusion between the borehole site and the region of primary crustal dilatation some20 km away. The return ("drainage") to the background state required more than a year.

Figure 4c. A pressure transient observed on the flank of the Juan de Fuca Ridge reveals thecontraction of the plate in response to a distant (110 km range) extensional spreading event likethat portrayed in Fig. 4b. A similar mixture of elastic response and hydraulic diffusion is seen inthis transient. Sites closer to basement outcrops where similar transients have been observeddisplay much shorter drainage time constants.

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Figure 4d. Pressure transientsassociated with a propagatingdislocation along the decollementseparating the Nankaiaccretionary prism from theunderthrusting Philippine Seaplate. Numbered monitoringlevels in the formation areordered according to theirposition above the decollement.The return to previousbackground levels (days to tens ofdays) takes place in far less timethan the drainage time constantthrough this thick sedimentarysection (tens to hundreds ofyears), indicating that thedislocation passed the site and leftlittle net strain. Dips belowbackground levels after passageof the positive pulses reflect aSquare Pants "squeegee" effect.

Figure 4e. "Chronic" contractional and extensional strain documented by positive and negativeformation-pressure trends in boreholes located 13 km apart in the subducting Philippine Seaplate and overriding Nankai accretionary prism, respectively, off southwestern Japan. Rates arecommensurate with those expected during inter-earthquake periods if inter-plate motion isabsorbed viscoelastically over a distance of tens of km. Pressure steps opposing the trends occurat the time of the transient shown in Fig. 4d, and reflect the deformation associated with thatevent.

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Figure 5. Two configurations of CORK (circulation obviation retrofit kit) borehole observatoriesconfigured for single- and multiple-zone formation monitoring.

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Figure 6. Schematic of multi-level “CORK-II” system and casing deployed in three holes duringIODP Expedition 301 and planned for two more holes in an approved but still unscheduled IODPrevisit. Primary CORK casing is 4-1/2” in diameter and is sealed with two plugs, one at depthand one at top. Additional seals are provided by casing packers and cement at base of the 16”and 10-3/4” main hole casing strings. Umbilicals running up the 4-1/2” casing allow forsampling from zone isolated beneath the packer at wellhead valves, for pressure monitoring andgeochemical/microbiological sampling. Only one casing packer is shown here, but someinstallations have/will have more casing packers, isolating and allowing for independentsampling from more than one downhole interval. Autonomous in-situ OsmSamplers andtemperature loggers are suspended on spectra rope within the central bore and below the bottomplug in open hole.

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Figure 7: The SeisCORK concept is to incorporate at least one VLF seismometer with atraditional CORK system in order to make simultaneous observations of seismicity with in situbiogeochemical and hydrogeological data. One goal is to study biogeochemical andhydrogeological events that may be associated (possibly as precursors) with earthquakes.

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Table 1. Existing and Proposed NEPTUNE Ocean Crustal Hydrogeology Sites.NEPTUNEHydrogeologySite number

ODP/IODPSite numberetc.

LatitudeLongitude

Approx.seafloordepth (m)

Monitoringlevels; overlap.Budget request intsunami prop = ++

H-1 857 48o 26.52' N128o 42.65' W

2500 Basement, sediment;Seis, Tsun

H-2 1024 47o 54.5' N128o 45.0' W

2600 Basement, sediment;Seis

H-3 1025 47o 53.3' N128o 39.0' W

2600 Basement, sediment;Seis

H-4 1029 47o 49.9' N128o 22.6' W

2600 Sediment;Seis

H-5a 1026 47o 45.76' N127o 45.55' W

2600 Basement

H-5b New approvedSR-2

47o 45.66' N127o 45.67' W

2600 Basement

H-5c 1301A/B(50 m apart)

47o 45.22' N127o 45.83' W

2600 Basement

H-5d 1027 47o 45.39' N127o 43.87' W

2600 Basement, sediment;Seis, Geod, Tsun++

H-5e Baby BareOutcrop

47o 42.6' N127o 45.83' W

2500 Seafloor experiments

H-6a Proposed 48o 14.0 ' N127o 32.0' W

2600 Sediment;Seis

H-6b Zona BareOutcrop

48o 11.3' N127o 33.0' W

2400 Seafloor experiments

H-7 Proposed 48o 34.0' N127o 10.0' W

2600 Sediment;Tsun++

H-8 889 48o 41.91' N126o 52.23' W

1400 Sediment;Seis, Hydrates,Tsun++

H-9 Proposed 48o 46.0' N126o 43.5' W

1100 Sediment;Tsun++

Note: Neptune Hydrogeology site numbers are ordered according to distance along the cross-plate transect from the ridge axis to the subduction zone. It is anticipated that experiments ateach sub-site (lettered) can be linked to a NEPTUNE interface site module via user-suppliedcables. Many of these sites will include pairs of holes completed in igneous basement and theoverlying sediment section, with holes separated by a few tens of metres. Instrumentation inmost basement holes will be already in place and will not require NEPTUNE funding. Budgetsfor installations at Tsunami sites (H-5 - H-9) are included in that proposal. Several sites willinclude buried broadband seismometers as described by the NEPTUNE Canada seismologygroup. An "absolute" (relative to North America) plate motion site will be established by theNEPTUNE Canada geodetic group at H-5 or H-6.

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8.0 References Cited and CORK Bibliography

8.1 References Cited

Baross, J., R. Carney, C. Fisher and K. Juniper. 1994. Hydrothermal vents and biodiversityworking group report; from RIDGE/VENTS Workshop on Global Impact of SubmarineHydrothermal Processes, Final Report; Sept. 11-13, 1994; Convenors: David Kadko, EdBaker, Jeff Alt and John Baross.

Becker, K. and E.E. Davis, in press, A review of CORK designs and operations during the OceanDrilling Program, Proc. IODP, Exp. Repts., 301.

Bohnenstiehl, D.R., M. Tolstoy, R.P. Dziak, C.G. Fox, and D.K. Smith (2002) Aftershocks in themid-ocean ridge environment: An analysis using hydroacoustic data. Tectonophysics 354, 49-70.

Cowen, J.P., S. Giovannoni, F. Kenig, H.P. Johnson, D. Butterfield, M. Rappe, M. Hutnak, and P.Lam (2003). Microorganisms in Fluids from 3.5 m.y. Ocean Crust. Science 299, 120-123.

Davis, E.E. and K. Becker. 1999. Tidal pumping of fluids within and from the oceanic crust: newobservations and opportunities for sampling the crustal hydrosphere. Earth Planet. Sci. Lett.172, 141-149.

Davis, E.E. and K. Becker, 2001, Using ODP boreholes for studying sub-seafloor hydrogeology:results from the first decade of CORK observations, Geoscience Canada, 28, 171-178.Fisher,A.T. and K. Becker. 2000. Channelized fluid flow in oceanic crust reconciles heat-flow andpermeability data. Nature 403, 71-74.

Davis, E.E., K. Becker, K. Wang, K. Obara, Y. Ito and M. Kinoshita, A discrete episode ofseismic and aseismic deformation of the Nankai subduction zone accretionary prism andincoming Philippine Sea plate, Earth Planet. Sci. Lett., in review.

Fisher, A.T., Wheat, C.G., Becker, K., Davis, E.E., Jannasch, H., Schroeder, D., Dixon, R.,Pettigrew, T.L., Meldrum, R., Macdonald, R., Nielsen, M., Fisk, M., Cowen, J., Bach, W.and 1Edwards, K., in press, Scientific and technical design and deployment of long-term,subseafloor observatories for hydrogeologic and related experiments, IODP Expedition 301,eastern flank of Juan de Fuca Ridge, Proc. IODP, Exp. Repts, 301.

Fisk, M.R., S.J. Giovannoni, I.H. Thorseth. 1998. Alteration of oceanic volcanic glass: texturalevidence of microbial activity. Science 281, 978-980.

Foucher, J.P., P. Henry, and F. Harmegnies, 1997, Long-term observations of pressure andtemperature in ODP Hole 948D, Barbados accretionary prism, Proc. ODP, Sci. Results, 156,239-245.

Furnes, H., I.H. Thorseth, O. Tumyr, T. Torsvik, M. Fisk. 1996. Microbial activity in thealteration of glass from pillow lavas from ODP Hole 896A, in : J.C. Alt, H. Kinoshita, L.B.Stokking, P.J. Michael (Eds.), Proc. ODP Sci. Res. 148, 191-206.

Furnes, H.I., K. Muehlenbachs, T. Torsvik, I.H. Thorseth and O. Tumyr. 2001. Microbialfractionation of carbon isotopes in altered basaltic glass from the Atlantic ocean, lau Basinand Costa Rica Rift. Chem. Geol. 173, 313-330.

Gold, T. 1992. The deep, hot biosphere. Proc. Natl. Acad. Sci. 89, 6045-6049.Johnson, H.P., M. Hutnak, R.P. Dziak, C. Fox, I. Urcuyo, J. Cowen, J. Nabelek, and C. Fisher, .

(2000). Earthquake-induced changes in a hydrothermal system on the Juan de Fuca mid-oceanridge. Nature 407: 174-177.

Kenig, F., Simons, D.-J. K., Crich, D., Cowen, J.P., Ventura, G.T., Rehbein-Khalily, T., Brown,T.C. (2003). Branched aliphatic alkanes with quaternary substituted carbon atoms in modern

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and ancient geologic samples. Proceedings of the National Academy of Sciences (PNAS)100, no. 22, 12554-12558.

Lilley, M.D., D.A. Butterfield, J.E. Lupton and E.J. Olson (2003) Magmatic events can producerapid changes in hydrothermal vent chemistry. Nature 422, 878-881.

Luther III, G. W., B. T. Glazer, et al. (2001). "Sulfur speciation monitored in situ with solid stategold amalgam voltammetric microelectrodes: polysulfides as a special case in sediments,microbial mats and hydrothermal vent waters." Journal of Environmental Monitoring 3(1):61-66.

Stephen, R.A., Pettigrew, T. L, et al, 2004, SeisCORK Meeting Report, WHOI Interval Report.Thorseth, I.H. and many. 2001. Diversity of life in ocean floor basalt. Earth Planet. Sci. Lett.

194, 31-37.Torsvik, T. H. Furnes, K. Muehlenbachs, I.H. Thorseth and O. Tumyr. 1998. Evidence for

microbial activity at the glass-alteration interface in oceanic basalts. Earth Planet. Sci. Letts.162, 165-176.

8.2 Appendix I. CORK publications as of November, 2004

I. Primary hardware descriptions

Davis, E.E., K. Becker, T. Pettigrew, B. Carson, and R. Macdonald, 1992, CORK: a hydrologicseal and downhole observatory for deep-ocean boreholes, Proc. ODP, Init. Repts., 139,43-53.

Jannasch, H.W., E.E. Davis, M.K. Kastner, J.D. Morris, T. L. Pettigrew, J. N. Plant, E.A.Solomon, H.W. Villinger, and C. G. Wheat, 2003, CORK-II: long-term monitoring offluid chemistry, fluxes, and hydrology in instrumented boreholes at the Costa Ricasubduction zone, Proc. ODP, Init. Repts., 205 (CD-ROM), 1-36.

Meldrum, R.D., Davis, E.E., Jones, G., and Macdonald, R.D., 1998. A two-way acousticcommunication link for deep-ocean observatories. Marine Tech. Soc. J., 32:24-31.

Shipboard Scientific Party, 2002, Explanatory Notes, In Mikada, H., Becker, K., Moore, J.C.,Klaus, A., et al., Proc. ODP, Init. Repts., 196 (CD-ROM), 1-53.

II. Primary CORK results

Becker, K. and E.E. Davis, 2003, New evidence for age variation and scale effects ofpermeabilities of young oceanic crust from borehole thermal and pressure measurements,Earth Planet. Sci. Lett., 210, 499-508.

Becker, K., A.T. Fisher, and E.E. Davis, 1997, The CORK experiment in Hole 949C: long-termobservations of pressure and temperature in the Barbados accretionary prism, Proc. ODP,Sci. Results, 156, 247-252.

Becker, K., A. Bartetzko, and E.E. Davis, 2001, Leg 174B synopsis: revisiting Hole 395A forlogging and long-term monitoring of off-axis hydrothermal processes in young oceaniccrust, Proc. ODP, Sci. Results, 174B, 1-13.

Becker, K., E.E. Davis, F.N. Spiess, and C.P. de Moustier, 2004, Temperature and video logsfrom the upper oceanic crust, Holes 504B and 896A, Costa Rica Rift flank: implicationsfor the permeability of upper oceanic crust, Earth Planet. Sci. Lett., 222, 881-896.

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Carson, B., M. Kastner, D. Bartlett, J. Jaeger, H. Jannasch, and Y. Weinstein, 2003, Implicationsof carbon flux from the Cascadia accretionary prism: results from long-term, in situmeasurements at ODP Site 892B, Marine Geology, 198, 159-180.

Cowen, J.P., S.J. Giovannoni, F. Kenig, H.P. Johnson, D. Butterfield, M.S. Rappe, M. Hutnak,and P. Lam, 2003, Fluids from aging ocean crust support microbial life, Science, 299,120-123.

Davis, E.E. and K. Becker, 1994, Formation temperatures and pressures in a sedimented rifthydrothermal system: ten months of CORK observations, Holes 857D and 858G, Proc.ODP, Sci. Results, 139, 649-666.

Davis, E.E. and K. Becker, 1999, Tidal pumping of fluids within and from the oceanic crust: newobservations and opportunities for sampling the crustal hydrosphere, Earth Planet. Sci.Lett., 172, 141-149.

Davis, E.E. and K. Becker, 2001, Using ODP boreholes for studying sub-seafloor hydrogeology:results from the first decade of CORK observations, Geoscience Canada, 28, 171-178.

Davis, E.E. and K. Becker, 2002, Observations of natural-state fluid pressures and temperaturesin young oceanic crust and inferences regarding hydrothermal circulation, Earth Planet.Sci. Lett., 204, 231-248.

Davis, E.E., K. Becker, K. Wang, and B. Carson, 1995, Long-term observations of pressure andtemperature in Hole 892B, Cascadia Accretionary Prism, Proc. ODP, Sci. Results, 146,299-311.

Davis, E.E., K. Wang, K. Becker, and R.E. Thomson, 2000, Formation-scale hydraulic andmechanical properties of oceanic crust inferred from pore-pressure response to periodicseafloor loading, J. Geophys. Res., 105, 13423-13435.

Davis, E.E., K. Wang, R.E. Thomson, K. Becker, and J.F. Cassidy, 2001, An episode of seafloorspreading and associated plate deformation inferred from crustal fluid pressure transients,J. Geophys. Res., 106, 21953-21963.

Davis, E.E., K. Becker, R. Dziak, J. Cassidy, K. Wang, and M. Lilley, 2004, Hydrologicresponse to a seafloor spreading episode on the Juan de Fuca Ridge, Nature, 430, 335-338.

Foucher, J.P., P. Henry, and F. Harmegnies, 1997, Long-term observations of pressure andtemperature in ODP Hole 948D, Barbados accretionary prism, Proc. ODP, Sci. Results,156, 239-245.

Screaton, E.J., B. Carson, and G.P. Lennon, 1995, Hydrogeological properties of a thrust faultwithin the Oregon accretionary prism, J. Geophys. Res., 100, 20025-20035.

Screaton, E.J., A.T. Fisher, B. Carson, and K. Becker, 1997, Barbados Ridge hydrogeologictests: implications for fluid migration along an active decollement, Geology, 25, 239-242.

Screaton, E.J., B. Carson, E.E. Davis, and K. Becker, 2000, Permeability of a decollement zone:results from a two-well experiment in the Barbados accretionary complex, J. Geophys.Res., 105, 21403-21410.

Wheat, C.G., H.W. Jannasch, M. Kastner, J.N. Plant, and E.H. DeCarlo. 2003. SeawaterTransport and reaction in upper oceanic basaltic basement: Chemical data fromcontinuous monitoring of sealed boreholes in a mid-ocean ridge flank environment. EarthPlanet. Sci. Lett., 216, 549-564, 2003.

Wheat, C.G., H.W. Jannasch, M. Kastner, J.N. Plant, E.H. DeCarlo, and G. Lebon. 2004.Venting Formation Fluids from Deep Sea Boreholes in a Ridge Flank Setting: ODP Sites1025 and 1026. Geochem. Geophys. Geosyst., submitted.

28

III. Studies constrained by CORK observations, syntheses using CORK results

Becker, K. and E.E. Davis, in press, In situ determinations of the permeability of the igneousoceanic crust, in Davis, E.E., Elderfield, H., eds, Hydrogeology of the OceanicLithosphere, Cambridge University Press.

Davis, E.E., and K. Becker, in press, Observations of Temperature and Pressure: Constraints onOcean Crustal Hydrologic State, Properties, and Flow in Davis, E.E., Elderfield, H., eds,Hydrogeology of the Oceanic Lithosphere, Cambridge University Press.Davis, E.E., Wang, K., and Becker, K., 2002, Comment on "Deep-penetration heat flow

probes raise questions about interpretations from shorter probes", Eos, Trans. AGU, 83, 196-197.Davis, E.E., K. Becker, and J. He, 2004, Costa Rica Rift revisited: constraints on shallow and

deep hydrothermal circulation in oceanic crust, Earth Planet. Sci. Lett., 222, 863-879.Davis, E.E., Wang, K., Becker, K., Thomson, R.E., and Yashayaev, I., 2003, Deep-ocean

temperature variations and implications for errors in seafloor heat flow determinations, J.Geophys. Res., 108, B1, 2034, doi:10.1029/2001JB001695.

Fisher, A., Geophysical constraints on hydrothermal circulation: observations and models, inEnergy and mass transfer in submarine hydrothermal systems, edited by P. Halbach, V.Tunnicliffe, and J. Hein, pp. 29-52, Dahlem University Press, Berlin, Germany, 2003.

Fisher, A., Rates and patterns of fluid circulation, in Hydrogeology of the Oceanic Lithosphere,edited by E.E. Davis, and H. Elderfield, pp. 339-377, Cambridge University Press,Cambridge, UK, 2004.

Fisher, A.T., K. Becker, and E.E. Davis, 1997, The permeability of young oceanic crust east ofJuan de Fuca Ridge determined using borehole thermal measurements, Geophys. Res.Lett., 24, 1311-1314.

Stein, J.S., and A.T. Fisher, Multiple scales of hydrothermal circulation in Middle Valley,northern Juan de Fuca Ridge: physical constraints and geologic models, J. Geophys. Res.,106 (B5), 8563-8580, 2001.

Stein, J.S., and A.T. Fisher, Observations and models of lateral hydrothermal circulation on ayoung ridge flank: reconciling thermal, numerical and chemical constraints, Geochem.,Geophys., Geosystems, 10.1029/2002GC000415, 2003.

Spinelli, G.A., and A.T. Fisher, Hydrothermal circulation within rough basement on the Juan deFuca Ridge flank, Geochem., Geophys., Geosystems, 5 (2), Q02001,doi:10.1029/2003GC000616, 2004.

Spinelli, G.A., L. Zühlsdorff, A.T. Fisher, C.G. Wheat, M. Mottl, V. Spiess, and E.G.Giambalvo, Hydrothermal seepage patterns above a buried basement ridge, eastern flankof the Juan de Fuca Ridge, J. Geophys. Res., 109, doi:10.1029/2003JB002476, 2004.

Wang, K. and E.E. Davis, 1996, Theory for the propagation of tidally induced pore pressurevariations in layered subseafloor formations, J. Geophys. Res., 101, 11483-11495.

Wang, K. and E.E. Davis, 2003, High permeability of young oceanic crust constrained bythermal and pressure observations, in M. Taniguchi, K. Wang, and T. Gamo, eds., Landand Marine Hydrogeology, Amsterdam: Elsevier, 165-188.

Wang, K., E.E. Davis, and G. van der Kamp, 1998, Theory for the effects of free gas in

subsea formations on tidal pore pressure variations and seafloor displacements, J. Geophys. Res.,

103, 12339-12353.

Wang, K., van der Kamp, G., and Davis, E.E., 1999. Limits of tidal energy dissipation by fluid

29

flow in subsea formations. Geophys. J. Int., 139, 763-768.

IV. Workshop reports, newsletter reports, cruise reports, articles for lay people

Becker, K. and E.E. Davis, 1997, CORK experiments: long-term observatories in

seafloor boreholes to monitor in-situ hydrologic conditions and processes, in (1) JAMSTEC

Journal of Deep Sea Research, Special Volume, 141-146, and (2) Proceedings of International

Workshop on Scientific Use of Submarine Cables, Okinawa, 69-74.

Becker, K. and E.E. Davis, 1998, Advanced CORKs for the 21st century, report of a

workshop sponsored by JOI/USSSP.Becker, K. and E.E. Davis, 1998, CORK reveals huge fluxes in off-axis hydrologic circulation,

JOI/USSAC Newsletter, 11(1), 12-15.Becker, K. and E.E. Davis, 2000, Plugging the seafloor with CORKs, Oceanus, 42(1), 14-16.Becker, K., J.-P. Foucher, and the ODPNaut scientific party, 1996, CORK string registers fluid

overpressure, JOI/USSAC Newsletter, 9(1), 12-15.Davis, E.E. and K. Becker, 1993, Studying crustal fluid flow with ODP borehole observatories,

Oceanus, 36(4), 82-86.Davis, E.E. and K. Becker, 1998, Borehole observatories record driving forces for hydrothermal

circulation in young oceanic crust, EOS, Trans. AGU, 79, 369, 377-378.Johnson, H.P. and the LEXEN Scientific Party, 2003, Probing for life in the ocean crust with the

LEXEN Program, EOS, Trans. AGU, 84, 109, 112.Mikada, H., Kinoshita, M., Becker, K., Davis, E.E., Meldrum, R.D., Flemings, P., Gulick, S.P.S.,

Matsubayashi, O., Morita, S., Goto, S., Misawa, N., Fujino, K., and Toizumi, M., 2003,Hydrogeological and geothermal studies around Nankai Trough (KR02-10 NankaiTrough Cruise Report), JAMSTEC J. Deep Sea Res., 22, 125-171.

Zierenberg, R., Becker, K., Davis, E., and the Leg 169 Scientific Party, 1996, Post-drillingexperiments and observations of a hydrothermal system, JOI/USSAC Newsletter, 9(3),16-19.

30

Preliminary Budget Justification

We start by noting several assumptions of sources of uncertainty in preparing ourprovisional budgets:

• The posted ORION RFA FAQ’s seem to indicate that costs to design and build thenecessary scientific instrumentation are not to be included in these proposed costs, but thelines of distinction are sometimes unclear.

• Thus, we presume that the basic scientific instrumentation costs, and scientific salarysupport, should then be sought from some combination of IODP and eventual ORIONscience funds.

• Therefore, we focus here on estimated costs of linkages to OOI infrastructure andengineering and ship support for this aspect.

• However, without a detailed engineering analysis or clear guidance from OOI operators,we as scientists are able to provide only order of magnitude estimates of these costs.

With those caveats, below are our estimates of the potential costs, based on a five-year budgetand broken down by the functions listed in section 5 of the project description:

• Consulting engineering to ensure physical compatibility with basic ODP/IODPoperational constraints and electronic compatibility with OOI operational constraints(subcontract to T. Pettigrew at Mohr Division of Stress Engineering) - $250k over 5 years

• Physical link-ups (“extension cables”) from boreholes to OOI nodes (NEPTUNE cablenodes or OOI buoy nodes) – unknown, cost estimates to be provided by OOI operators?

• Design and construction of OOI-compatible communications system for pressure dataloggers - $50k plus $25k per installation

• Design and construction of downhole temperature strings with signal conditioning andcommunication via OOI protocols – partially an instrumentation cost, linkage to OOIinfrastructure at $50k plus $25k per installation

• Design and construction of downhole fluid and microbiological analyzers compatiblewith OsmoSamplers and OOI communication protocols - partially an instrumentationcost, linkage to OOI infrastructure at $50k plus $25k per installation

• Design and construction of SeisCORK 1-100 Hz downhole monitoring and seafloorrecording system compatible with OOI communication protocols - partially aninstrumentation cost, linkage to OOI infrastructure at $100k plus $50k per installation

• Design and construction of wellhead fluid/microbiological sampling system compatiblewith OOI communication protocols - partially an instrumentation cost, linkage to OOIinfrastructure at $100k plus $50k per installation

This breaks down to estimated fixed engineering costs of $600k over five years plus estimatedper installation costs as high as $175k for a borehole observatory that incorporates the full rangeof downhole and seafloor instrumentation. However, for the NEPTUNE borehole array, most ofthe 14 sites listed in Table 1 will each incorporate only a subset of the instrumentation, and auseful first-order estimate of the average per installation cost to link to OOI might be $100k. Ifall 14 NEPTUNE sites are instrumented, the net cost for linking all to the OOI infrastructurewould then be ~$1.4M. Of the fixed engineering costs, $250k is listed as as a subaward to MohrDivision of Stress Engineering, and the remaining $350k would be distributed as engineeringsupport within proponent institutions. Finally, travel of PI’s and engineers will certainly berequired in the design process, and we estimate a total of $50k over the 5 year duration.

CUMULATIVE PROPOSAL BUDGET

FOR ORION USE ONLY

ORGANIZATION

Split among proponent institutions over 5 yearsPROPOSAL NO. DURATION (MONTHS)

Proposed Granted

PRINCIPAL INVESTIGATOR/PROJECT DIRECTOR

K. Becker and co-proponentsAWARD NO.

A. SENIOR PERSONNEL: PI/PD, Co-PIs, Faculty and Other Senior Associates Funded Funds Funds

List each separately with name and title. (A.7. Show number in brackets) Person-months Requested By Granted

CAL ACAD SUMR Proposer (If Different)

1. _____ __ __ __ $_____ $_____ 2. _____ __ __ __ _____ _____ 3. _____ __ __ __ _____ _____ 4. _____ __ __ __ _____ _____ 5. _____ __ __ __ _____ _____ 6. (___) OTHERS (LIST INDIVIDUALLY ON BUDGET EXPLANATION PAGE) __ __ __ _____ _____ 7. (___) TOTAL SENIOR PERSONNEL (1-6) __ __ __ _____ _____B. OTHER PERSONNEL (SHOW NUMBERS IN BRACKETS)

1. (___) POSTDOCTORAL ASSOCIATES __ __ __ _____ _____ 2. (?) OTHER PROFESSIONALS (TECHNICIAN, PROGRAMMER, ETC.) __ __ __ $350,000 _____ 3. (___) GRADUATE STUDENTS _____ _____ 4. (___) UNDERGRADUATE STUDENTS _____ _____ 5. (___) SECRETARIAL - CLERICAL (IF CHARGED DIRECTLY) _____ _____ 6. (___) OTHER _____ _____ TOTAL SALARIES AND WAGES (A + B) _____ _____C. FRINGE BENEFITS (IF CHARGED AS DIRECT COSTS) _____ _____ TOTAL SALARIES, WAGES AND FRINGE BENEFITS (A + B + C) _____ _____D. EQUIPMENT (LIST ITEM AND DOLLAR AMOUNT FOR EACH ITEM EXCEEDING $5,000.)

Per installation costs of $100k for 14 borehole installations__________ TOTAL EQUIPMENT $1,400,000 _____E. TRAVEL 1. DOMESTIC (INCL. CANADA, MEXICO AND U.S. POSSESSIONS) $50,000 _____

2. FOREIGN _____ _____F. PARTICIPANT SUPPORT 1. STIPENDS $ _____ 2. TRAVEL _____ 3. SUBSISTENCE _____ 4. OTHER _____ TOTAL NUMBER OF PARTICIPANTS (_____) TOTAL PARTICIPANT COSTS _____ _____G. OTHER DIRECT COSTS _____ _____ 1. MATERIALS AND SUPPLIES _____ _____ 2. PUBLICATION/DOCUMENTATION/DISSEMINATION _____ _____ 3. CONSULTANT SERVICES _____ _____ 4. COMPUTER SERVICES _____ _____ 5. SUBAWARDS subcontract to Mohr Division of Stress Engineering $250,000 _____ 6. OTHER _____ _____ _____ TOTAL OTHER DIRECT COSTS _____ _____H. TOTAL DIRECT COSTS (A THROUGH G) _____ _____I. INDIRECT COSTS (F&A) (SPECIFY RATE AND BASE)

Estimate 50% of modified indirect costs of $650,000 = $325,000_____ TOTAL INDIRECT COSTS (F&A) $325,000 _____J. TOTAL DIRECT AND INDIRECT COSTS (H + I) $2,375,000 _____K. RESIDUAL FUNDS (IF FOR FURTHER SUPPORT OF CURRENT PROJECT SEE GPG II.D.7.j.) _____ _____L. AMOUNT OF THIS REQUEST (J) OR (J MINUS K) $2,375,000 $_____M. COST SHARING: PROPOSED LEVEL $_____ AGREED LEVEL IF DIFFERENT: $_____PI/PD TYPED NAME AND SIGNATURE* DATE FOR ORION USE ONLY

INDIRECT COST RATE VERIFICATION

ORG. REP. TYPED NAME & SIGNATURE* DATE Date Checked Date of Rate Sheet Initials-ORG

_____ _____

OOI Form 1030 (10/99) Supersedes All Previous Editions *SIGNATURES REQUIRED ONLY FOR REVISED BUDGET (GPG III.C)

KEIR BECKER - SHORT CV

Birth: 27 March 1951, Chicago, Illinois, USA

Address: Division of Marine Geology & Geophysics, University of Miami, Miami, FL 33149

kbecker@rsmas.miami.edu, 305-361-4661

Education and Position Held:

A.B., 1975, Physical Sciences cum laude, Harvard CollegePh.D., 1981, Oceanography, Scripps Institution of Oceanography, University of CaliforniaAssistant Research Geophysicist, Deep Sea Drilling Project and Geological Research

Division, Scripps Institution of Oceanography, 1981-1986Assistant Professor, RSMAS - MGG, University of Miami, 1985-1987Associate Professor, RSMAS - MGG, University of Miami, 1987-1994Professor, RSMAS - MGG, University of Miami, 1994-present

Scientific Expeditions since 1990 (* = Chief or Co-Chief Scientist):

(Prior to 1990: DSDP Legs 70, 78B, 83, 92; ODP Legs 102, 109, 111*, 118)1991 ODP Legs 137 *, 139; Atlantis II 125-321993 ODP Leg 148; Atlantis II 129-5; Atlantis II 131-4 *1994 Atlantis II 131-18; ODP Leg 1581995 Atlantis II 132-10 *; ODPNAUT I *1996 ODP Leg 1681997 ODP Leg 174B *; Atlantis 3-8 *1998 ODPNAUT II *1999 Atlantis 3-39 *2000 ODP Leg 190, Revelle Nalu01, Atlantis 3-55 *2001 ODP Leg 196 *, Revelle Drift03 *2002 JAMSTEC Kairei KR02-10, Atlantis 7-25 *2003 JAMSTEC Kairei KR03-052004 JAMSTEC Yokosuka YK04-05, IODP Expedition 301

Committee Service

JOIDES (DSDP/ODP) Downhole Measurements Panel, 1982-1990Science Experiments Committee, Salton Sea Scientific Drilling Project, 1984-1985JOIDES Tectonics Panel, 1984-1986JOIDES Lithosphere Panel, 1986-1990U.S. Science Advisory Committee for ODP (USSAC), 1988-1990USSAC Executive Committee, 1989-1990JOIDES Planning Committee, 1990-1994RIDGE Steering Committee, 1994-1997Chairman, JOIDES Engineering Development Review Committee, 1994BOREHOLE Steering Committee, 1994-1997Co-Chairman, DEOS Steering Committee, 1997- 2000Co-Chairman, JOIDES Long-Term Observatory PPG, 1997-1999NAS/NRC Committee on Seafloor Observatories, 1999-2000DEOS/OOI Steering Committee, 2001-Chairman, JOIDES Science Committee, 2001-2003Chairman, JOIDES Operations Committee, 2001-2003WHOI New Alvin Design Advisory Committee, 2002-2003NAS/NRC Committee on Future Needs in Deep Submergence Science, 2003IODP Science Planning Committee, 2003-2007

Vice-chair, 2004-2005; Chair-nominee, 2005-2007

Convenor and Steering Committee Service, Conferences and Workshops (* = USSAC funding)

Co-convenor, SCORE (Sediment-Covered Ocean Ridges Experiments) Workshop, 1994 *Co-convenor, OBLISP [BOREHOLE] Workshop, 1994 *Steering Committee, ION Workshop, 1995Co-convenor, Advanced CORK Workshop, 1997 and 1998 *Co-convenor, Workshop on Hydrogeology of Oceanic Lithosphere, 1998 *Steering Committee, DESCEND Workshop, 1999Convenor, CORK mini-workshop, 2004 *

Some Recent, ODP-Related Open-Literature Publications

Davis, E.E. and Becker, K., 1993, Studying crustal fluid flow with ODP borehole observatories,Oceanus, 36(4), 82-86.

Screaton, E.J., Fisher, A.T., Carson, B., and Becker, K., 1997, Barbados Ridge hydrogeologictests: implications for fluid migration along an active decollement, Geology, 25, 239-242.

Davis, E.E. and Becker, K., 1999, Tidal pumping of fluids within and from the oceanic crust: newobservations and opportunities for sampling the crustal hydrosphere, Earth Planet. Sci.Lett., 172, 141-150.

Becker, K. and Davis, E.E., 2000, Plugging the Seafloor with CORKs, Oceanus, 42, 14-16.Becker, K., and DEOS Steeering Committee, Seeding the oceans with observatories, Oceanus,

42(1), 2-5.Screaton, E., Carson, B., Davis, E., and Becker, K., 2000, Permeability of a decollement zone:

results from a two-well experiment in the Barbados accretionary complex, J. Geophys.Res., 105, 21,403-21, 410.

Becker, K., and Fisher, A.T., Permeability of upper oceanic basement on the eastern flank of theJuan de Fuca Ridge determined with drill-string packer experiments, J. Geophys. Res.,105, 897-912.

Fisher, A.T., and Becker, K., Channelized fluid flow in oceanic crust reconciles heat-flow andpermeability data, Nature, 403, 71-74.

Davis, E.E., Wang, K., Becker, K., and Thomson, R., 2000, Formation-scale hydaulic andmechanical properties of oceanic crust inferred from pore-pressure response to periodicseafloor loading, Journal of Geophysical Research, 105, 13,423-13,435.

Davis, E.E., Wang, K., Thomson, R.E., Becker, K., and Cassidy, J.F., An episode of seafloorspreading and associated plate deformation inferred from crustal fluid pressuretransients, Journal of Geophysical Research, 106, 21,953-21,964, 2001.

Hay, W.W. and Becker, K., Ocean Drilling Program’s research intensifies as end nears, Eos,Trans. AGU, 82, 201, 209, 2001.

Becker, K., Ocean Drilling Program plans final year of operations, Eos, Trans. AGU, 83, 157, 159,2002.

Davis, E.E., and Becker, K., Observations of natural-state fluid pressures and temperatures inyoung oceanic crust and inferences regarding hydrothermal circulation, Earth Planet. SciLett., 204, 231-248, 2002.

Becker, K., and Davis, E.E., New evidence for age variation and scale effects of permeabilities ofyoung oceanic crust from borehole thermal and pressure measurements, Earth Planet.Sci. Lett., 210, 499-508, 2003.

Davis, E.E., Becker, K., and He, J., Costa Rica Rift revisited: constraints on shallow and deephydrothermal circulation in oceanic crust, Earth Planet. Sci. Lett., 222, 863-879.

Becker, K., Davis, E.E., Spiess, F.N., and deMoustier, C.P., Temperature and video logs from theupper oceanic crust, Holes 504B and 896A, Costa Rica Rift flank: implications for thepermeability of upper oceanic crust, Earth Planet. Sci. Lett., 222, 881-896.

Davis, E.E., Becker, K., Dziak, R., Cassidy, J., Wang, K., and Lilley, M., Hydrological response to aseafloor spreading regime on the Juan de Fuca ridge, Nature, 430, 335-338.

JAMES PRATHER COWEN

PERSONAL DATA

Department of Oceanography

School of Ocean and Earth Science and Technology Birthdate: March 11, 1951

University of Hawaii Married; 2 Children

1000 Pope Road, MSB 307 (808) 956-7124

Honolulu, HI 96822 (808) 262-6270 (home)

jcowen@soest.hawaii.edu (808) 956-9225 (fax)

EDUCATION

Ph.D. Biology (Oceanography); University of California, Santa Cruz 1983

M.A. Biology; University of California, Santa Barbara 1976

B.A. Environmental Biology (Honors); University of California, Santa Barbara 1973

RESEARCH EXPERIENCE

1998-Present Research Professor, Department of Oceanography

1991-1998 Associate Research Professor, Department of Oceanography

1991-Present Graduate Faculty of Department of Oceanography, University of Hawaii

1990-1991 Associate Research Geochemist, Hawaii Institute of Geophysics, UH

1986-1990 Assistant Research Geochemist, Hawaii Institute of Geophysics, UH

1986-Present Graduate Faculty, UH

1984-1985 National Research Council Research Associate, NOAA, Pacific

Marine Environmental Laboratory, Seattle, Washington.

FIELD INVESTIGATIONS: Participated in over 34 research cruises (>5 days), Chief or Co-chief

Scientist on 14

SYNERGISTIC ACTIVITIES (in addition to Graduate and Undergrad. instruction)

2005-Lecturer, NAI Winter School on Astrobiology, Jan. 10-21, 2005; Honolulu and Hilo, HI

2002-Panelist, NSF Panel for Geoscience CAREER; Nov. 20-22, 2002; Washington, D.C.

2001-2003: Executive Committee, RIDGE 2000 Program

2001-Present: PI of “Teacher at Sea” component of NSF Chem. Ocean. research project.

1989-Present: Active Role in educating/activating scientific and administrative community

capability to rapidly respond to mid-ocean ridge volcanic events.

1994-1998, 2000-2003: RIDGE Steering Committee member, a NSF Program

1988-Present: Science outreach to k-12 school children (Class room lectures/ demonstrations;

yearly Hawaiian Science and Engineering Fair Judge; Host/Moderator of high school Annual

Student Symposium; Ship-to-Classroom email projects)

OTHER RECENT PROFESSIONAL ACTIVITIES

2004- Associate Editor, Journal Geophysical Research—Biogeochemistry

Organizing Committee, NASA Astrobiology Institute 2005 Biennium Meeting, Boulder,

Colorado, April 11-14, 2005

Proposal Review Panel: Sea Grant Hawaii proposal, April, 2004.

2003- Chair, Organizing Committee, Ridge2000 Community Workshop; Denver, Colorado;

November, 2003.

Participant, Workshop on “Next Generation of Biological and Chemical Sensors in the

Ocean”; WHOI, Woods Hole, MA; July 13-16, 2003

Participant, Workshop on “Linkages Between the Ocean Observatories Initiative and the

Integrated Ocean Drilling Program”, Seattle, WA; July 17-18, 2003.

2002-Speaker/participant: MOMAR II (Workshop on International Sea-Floor Observatory on

the Mid-Atlantic Ridge) Horta, Faial Island, Azores, Portugal. June, 2002

Invited participant: InterRidge: The Next 10 Years; Bremen, Germany; June, 2002

2001- Invited participant and Invited author of Background position paper Dahlem Conference

on “Energy and Mass Transfer in Marine Hydrothermal Systems”,; Berlin, Germany,

October 14-19, 2001.

2000-Organizing committee: Integrated Studies Workshop, planning for new RIDGE-2000

Invited participant: National Research Council Seafloor Observatory Symposium,

Islamorada, Florida. Jan. 9-13, 2000.

1999- Invited participant: NEPTUNE Science Working Group;. Aug/Sept, ‘99

Session chair: DESCEND meeting; Washington, D.C.; Oct. 25-27, ‘99

Visiting scholar: Japanese RIDGEFLUX Program, Institute of Ocean Research Institute

(U. of Tokyo), Kyushu U., and Geological Survey of Japan; March, ‘99.

10 RELEVANT PUBLICATIONS

Kenig F., Simons D.-J.H., Ventura G.T. , Crich D., Cowen J.P., Rehbein-Khalily T. (2005)

Structure and distribution of branched-alkanes with quaternary carbon atoms in Cenomanian

and Turonian black shales of Pasquia Hill (Saskatchewan, Canada). Organic Geochemistry

36, 1, 117-138

Cowen, J.P. (2004) The Microbial Biosphere of Sediment-Buried Oceanic Basement.

Research in Microbiology 155/7: 497-506

Cowen, J.P., E.T. Baker, and R.W. Embley (2004). Detection of and Response to Mid-ocean

ridge magmatic/tectonic events: implications for the subsurface biosphere. In: RIDGE

Theoretical Institute: The SubseaFloor Biosphere at Mid-Ocean Ridges; Edited by: W.

Wilcock, C. Cary, E. DeLong, D. Kelley, and J. Baross. (In Press)

Lam, P., Cowen, J.P., and Jones, R. (2004). Autotrophic ammonia oxidation in a hydrothermal

plume. FEMS Microbiology and Ecology 47, 191-206.

Cowen, J.P., S. Giovannoni, F. Kenig, H.P. Johnson, D. Butterfield, M. Rappe, M. Hutnak, and

P. Lam (2003). Microorganisms in Fluids from 3.5 m.y. Ocean Crust. Science 299, 120-

123.

Cowen, J.P. and C. German (2003) Biogeochemical Cycling in Hydrothermal Plumes; In:

Energy and Mass Transfer in Marine Hydrothermal Systems, Halbach, P.E.,

Tunnicliffe, V. and Hein, J.R., eds. 2003 Dahlem University Press.

Cowen, J.P., X. Wen, B.N. Popp (2002). Methane in Aging Hydrothermal Plumes. Geochim.

Cosmochim. Acta 66: 3563-3571

Cowen, J.P., M. Bertram, S. Wakeham, R.E. Thomson, J.W. Lavelle, E.T. Baker, and R.A.

Feely (2001). Ascending particle flux from a hydrothermal plume: biogeochemical linkages

with the upper water column. Deep Sea Research I 48(4):1093-1120.

Johnson, H.P., M. Hutnak, R.P. Dziak, C. Fox, I. Urcuyo, J. Cowen, J. Nabelek, and C. Fisher, .

(2000). Earthquake-induced changes in a hydrothermal system on the Juan de Fuca mid-

ocean ridge. Nature 407: 174-177.

Cowen, J.P., M.A. Bertram, E.T. Baker, G.J. Massoth, R.A. Feely, and M. Summit (1998)

Geomicrobial Transformation of Manganese in Gorda Ridge Event Plumes. Deep Sea Res.

II 45: 2713-2738.

Other Collaborators: H.Paul Johnson (UW), B. Burd, F. Sansone, Geoff Wheat, M. Mottl, S.

Giovannoni, F. Kenig, B. Popp, C. Winn, M. Rappe, D. Kadko

Graduate Advisor: K. Bruland; Graduate Students: M. Bertram, J. Christian, C. Holloway, M.

Irving, P. Lam , J. Marsters, R. Shackelford, X. Wen, Y. Plancherel

BIOGRAPHICAL SKETCH

Earl Edwin DavisPacific Geoscience CentreGeological Survey of CanadaP.O. Box 6000 / 9860 W. Saanich Rd.Sidney, B.C. V8L 4B2 CanadaE-mail: davis@pgc.nrcan.gc.ca

Birth: 1947 May 18, Oceanside, California, USACitizenship: Canadian/U.S.

Education and positions held:B.Sc., Physics, University of California, Santa Barbara, 1969Ph.D., Geophysics, University of Washington, 1975Ida and Cecil Green Post-Doctoral Fellow, Massachusetts Institute of Technology, 1975-1977Visiting Lecturer, Oregon State University, 1977Research Associate, Victoria Geophysical Observatory, 1977-79Visiting Scientist, University of Washington, 1979-80Research Scientist, Geological Survey of Canada, 1980-present

Research interestsHydrothermal circulation, mid-ocean ridges, ocean crustal hydrogeology, subduction zone

accretionary prism structure and hydrology, heat flow, marine geophysical instrumentation

Recent scientific expeditions (* = chief or co-chief scientist)1991 JOIDES Resolution, ODP Leg 139 *1991 RV Atlantis II/DSV Alvin CORK data recovery, JFR1992 CHS Tully, Juan de Fuca Ridge flank hydrothermal circulation *1993 RV Atlantis II/DSV Alvin, CORK data recovery, Cascadia accretionary prism1995 CHS Tully, Juan de Fuca Ridge flank hydrothermal circulation (chief scientist)1996 JOIDES Resolution, ODP Leg 168 (co-chief scientist)1997 RV Atlantis/DSV Alvin, CORK data recovery, JFR flank1998 RV Nadir/DSV Nautille, CORK data recovery, Barbados prism and Mid-Atlantic Ridge1998 RV Atlantis/DSV Alvin, CORK data recovery, JFR flank1999 RV Atlantis/DSV Alvin/Wireline Control Vehicle, CORK operations, JFR flank2000 RV Roger Revelle, Wireline Control Vehicle, Wireline CORK engineering tests2000 RV Thomas Thompson, RetroFlux * JFR flank2001 JOIDES Resolution, ODP Leg 196, Nankai Trough Advanced CORKs2001 RV Roger Revelle, Wireline CORK deployments, Holes 504B and 896A2002 RV Kairei/ROV Kaiko, Advanced CORK data recovery, Nankai accretionary prism2002 RV Atlantis/DSV Alvin, CORK data recovery, Costa Rica Rift and Costa Rica margin2003 RV Kairei/ROV Kaiko, Advanced CORK data recovery, Nankai accretionary prism2003 RV Thompson/ROV Jason II, CORK operations, JFR axis and flank

Awards1995 American Geophysical Union Editor's Citation for Excellence in Reviewing1996 Geological Association of Canada M.J. Keen Award, Marine Geoscience

Recent committees and community contributions1988-92 Associate editor, Marine Geology1988-92 Member, ROV development committee, Institute of Ocean Sciences1988- Member, Canadian National Committee, Ocean Drilling Program1989-93 Member, International Council of Scientific Union's Scientific Committee on Oceanic

Research, Hydrothermal Emanations at Plate Boundaries working group1993-96 Member, NSERC Shiptime Allocation Committee1994-95 Chairman, NSERC Shiptime Allocation Committee1997-98 Member, Observatories Planning Group, ODP1997-98 Member, Northeast Pacific Time-series Undersea Cabled Network Steering Comm.1998- Co-chair, International Lithosphere Program on Hydrology of the Oceanic Lithosphere1999-2000 Member, Science Working Group, Integrated Ocean Drilling Program1999- Member, Hydrogeology Planning Group, ODP1999- Associate Editor, Journal of Geophysical Research

Ten most relevant recent publications:

Davis, E.E., Becker, K., Pettigrew, T., Carson, B., and MacDonald, R., CORK: A hydrologic seal anddownhole observatory for deep ocean borholes, in Davis, E.E., Mottl, M.J., Fisher, A.T., Proceedingsof the Ocean Drilling Program, Initial Reports, v. 139, 43-53, 1992.

Wang, K., and Davis, E.E., Theory for the propagation of tidally induced pore pressure variations inlayered subseafloor formations, Journal of Geophysical Research, 101, 11483-11495, 1996.

Fisher, A.T., Becker, K., and Davis, E.E., The permeability of young oceanic crust east of Juan de FucaRidge determined using borehole thermal measurements, Geophysical Research Letters, 24, 1311-1314, 1997.

Davis, E.E., and K. Becker, Tidal pumping of fluids within and from the oceanic crust: New observationsand opportunities for sampling the crustal hydrosphere, Earth and Planetary Science Letters, 172,141-149, 1999.

Davis, E.E., Wang, K., Becker, K., and Thomson, R., Formation-scale hydraulic and mechanicalproperties of oceanic crust inferred from pore-pressure response to periodic seafloor loading,Journal of Geophysical Research, 105, 13,423-13,435, 2000.

Davis, E.E., Wang, K., Becker, K., and Thomson, R.E., An episode of seafloor spreading and associatedplate deformation inferred from crustal fluid pressure transients, Journal of Geophysical Research,106, 21953-21,963, 2001.

Davis, E.E., and Becker, K., Observations of natural-state fluid pressures and temperatures in youngoceanic crust and inferences regarding hydrothermal circulation, Earth Plan. Sci. Lett., 204, 231-248, 2002.

Becker, K., and Davis, E.E., New evidence for age variation and scale effects of permeabilities of youngoceanic crust from borehole thermal and pressure measurements, Earth Plan. Sci. Lett., 210, 499-508, 2003.

Davis, E.E., Becker, K., and He, J., Costa Rica Rift revisited: Constraints on shallow and deephydrothermal circulation in oceanic crust, Earth Plan. Sci. Lett., submitted, 2003.

Davis, E.E., and Elderfield, H., (eds.), Hydrogeology of the Oceanic Lithosphere, Cambridge UniversityPress, in press, 2003.

Andrew T. Fisher

Earth Sciences Department, A209 (831) 459-5598 (direct)University of California, Santa Cruz (831) 459-4089 (main office)1156 High Street (831) 459-3074 (fax)Santa Cruz, CA 95064 afisher@ucsc.edu

Education:1984-89 Ph. D., University of Miami, Marine Geology and Geophysics1980-84 B. S., Stanford University, Geology

Positions Held:2003-

1999-031995-991994-951993-95

19931989-931989-931988

Professor

Associate ProfessorAssistant ProfessorGraduate FacultyAssociate Scientist

Visiting Assistant ProfessorAdjunct Assistant ProfessorStaff ScientistExploration Geologist

Department of Earth Sciences, UCSC; also Institute forGeophysics and Planetary PhysicsDepartment of Earth Sciences, UCSCDepartment of Earth Sciences, UCSCDepartment of Geological Sciences, Indiana UniversityDepartment of Geological Sciences and Indiana GeologicalSurveyDepartment of Geophysics, Texas A & M UniversityDepartment of Geophysics, Texas A & M UniversityOcean Drilling Program, Texas A & M UniversityShell Western E & P, Inc.

Selected Synergistic Activities:• Teaches courses in Hydrology, Groundwater, Geological Principles, and Groundwater

Modeling• Member of technical advisory committees (volunteer) for Soquel Creek Water District,

Pajaro ValleyWater Management Agency, County of Santa Cruz Resource ConservationService, Monterey County Water Resources AgencySupervised 25 undergraduate researchers during 2000-04, including seven REU scholars;UCSC EarthSciences Department undergraduate faculty advisor, 1998-2001Twenty-four invited presentations during 2000-04, including four to non-scientific groups

• Editorial boards (1997-03) of Geology, Journal of Geophysical Research, Geofluids, TheIsland Arc

• Eight ODP/IODP expeditions, 10 other oceanographic expeditions, six as chief or co-chiefscientist

• ODP/IODP service: SPC, iPC, SCICOM, LITHP, DMP, USSAC, COMPLEX, CONCORD

Five recent references related to proposed research:Fisher, A. T., Rates and patterns of fluid circulation, in Hydrogeology of the Oceanic

Lithosphere, edited by Davis, E. E., and H. Elderfield, Cambridge University Press,Cambridge, UK, 339-377.

Wilcock, W.S.D., and A. T. Fisher, Geophysical constraints on the sub-seafloor environmentnear mid-ocean ridges, in Subseafloor Biosphere at Mid-ocean Ridges, Geophys.Monogr. Ser., 144, ed. by C. Cary, E. Delong, D. Kelley, W.S.D. Wilcock, American

Geophysical Union, Washington, D. C., 51-74.Spinelli, G.A., and Fisher, A. T., Hydrothermal circulation within rough basement on the Juan de

Fuca Ridge flank, Geochem., Geophys., Geosystems, 5 (2), Q02001,doi:10.1029/2003GC000616, 2004.

Fisher, A., E.E. Davis, Hutnak, M., Spiess, V., Zühlsdorff, L., Cherkaoui, A., Christiansen, L.,Edwards, K.M., Macdonald, R., Villinger, H., Mottl, M., Wheat, C. G., and Becker, K.,2003, Hydrothermal circulation across 50 km on a young ridge flank: the role ofseamounts in guiding recharge and discharge at a crustal scale, Nature, 421: 618-621,2003.

Stein, J.S., and Fisher, A. T., Observations and models of lateral hydrothermal circulation on ayoung ridge flank: reconciling thermal, numerical and chemical constraints, Geochem.,Geophys., Geosystems, 4 (3), 10.1029/2002GC000415, 2003.

Becker, K, and Fisher, A. T., 2000, Permeability of upper oceanic basement on the eastern flankof the Endeavor Ridge determined with drill-string packer experiments, J. Geophys. Res.,105 (B1): 897-912.

Five other recent references:Harris, R. N., Fisher, A. T., Chapman, D., Seamounts induce large fluid fluxes, Geology, 32 (8),

725728, doi:10.1130/G20387.1, 2004.Fisher, A. T., Stein, C. A., Harris, R. N, Wang, K., Silver, E. A., Pfender, M., Hutnak, M.,

Cherkaoui, A., Bodzin, R., Villinger, H., Abrupt thermal transition reveals hydrothermalboundary and role of seamounts within the Cocos Plate, Geophys. Res. Lett., 30 (11),1550, doi:10.1029/2002GL016766, 2003.

Fisher, A. T., and Becker, K., Reconciling heat flow and permeability data with a model ofchannelized flow in oceanic crust, Nature, 403: 71-74, 2000.

Stein, J., and Fisher, A. T., 2001. Multiple scales of hydrothermal circulation in Middle Valley,northern Juan de Fuca Ridge: physical constraints and geologic models, J. Geophys. Res.,106: 8563-8580.

Giambalvo, E., Fisher, A. T., Martin, J., Darty, L., and Lowell, R., Origin of elevated sedimentpermeability in a hydrothermal seepage zone, eastern flank of the Juan de Fuca Ridge,and implications for transport of fluid and heat, J. Geophys. Res., 105 (B1): 913-927.

Collaborators in last 48 months (other than co-authors listed above):Constantz, J. (USGS); Silver, E. (UCSC); Spiess, V. (Univ. Bremen); Sclater, J. (UCSD),

Zühlsdorff, L. (Univ. Bremen); Mottl, M. (Hawaii); Urabe, T. (Tokyo); Bach, W. (WHOI).

Graduate Advisor of co-PI: Becker, K. (University of Miami)

Graduate Advisees of co-PI:Christine Hatch, Mike Hutnak, Robert Sigler, Greg Stemler, Chris Ruehl (M.S., 2004),

Patrice Friedmann (M.S., 2003), Glenn Spinelli (Ph.D., 2002), Emily Giambalvo (Ph.D., 2001),Joshua Stein (Ph.D., 2000), Danielle Widemann (CW M.S., 2000), Jonathan Lear (CW M.S.,2000), Jon Erskine (M.S., 1998)

Post-doctoral Researchers supervised by co-PI:Abdellah Cherkaoui (2000-02), Philip Stauffer (1999)

Ralph Archibald Stephen

Marine Geophysicist Telephone: (508) 289-2583

Senior Scientist Fax: (508) 457-2150

Department of Geology and Geophysics E-mail: rstephen@whoi.edu

Woods Hole Oceanographic Institution Home Page: http://msg.whoi.edu/msg.html

Woods Hole, MA 02543

Date of Birth: 18 February, 1951

Place of Birth: Toronto, Canada

Nationality: USA (Naturalized, 1989)

PROFESSIONAL PREPARATION:

University of Toronto, Engineering Science, B.A.Sc. (Hon) 1974

University of Cambridge, Geodesy and Geophysics, Ph.D. 1978

APPOINTMENTS:

Senior Scientist, WHOI, November 1990 to present

Associate Scientist with tenure, WHOI, June 1986 to November 1990

Associate Scientist, WHOI, June 1982 to May 1986

Assistant Scientist, WHOI, June 1978 - May 1982

RESEARCH INTERESTS:

Marine seismology and geoacoustics, Seismic structure of oceanic crust, Seismic wave

propagation in heterogeneous media, Borehole seismic experiments, Finite difference synthetic

seismograms, VLF and ULF ambient noise in the ocean bottom, Broadband seismology,

Seismometry

RECENT OUTSIDE COMMITTEES AND ACTIVITIES:

Ocean Seismic Network Steering Committee - December 1995 - present

International Ocean Networks (ION - participant) - June 1993 - present

IRIS Board of Directors - February 1996 - present

LDEO-Borehole Research Group Board - December 1998 - October 2003

AGU Meetings Committee - July 2000 - June 2004

Associate Editor, Journal of the Acoustical Society of America, January 2002 - present

RECENT CRUISES:

R/V THOMAS THOMPSON - January/February 1998 - Chief Scientist - OSN Pilot

Experiment Deployment Cruise

R/V MELVILLE - June 1998 - Chief Scientist - OSN Pilot Experiment Recovery Cruise

D/V JOIDES RESOLUTION - December 2001/January 2002 - ODP Leg 200 - Co-Chief

Scientist - Nuuanu Landslide (at Site 1223) and Hawaii-2 Observatory (at Site 1224)

KAIREI - October 2002 - Visiting Scientist - Data recovery cruise to WP-1

RECENT IN-HOUSE ACTIVITIES:

Senior/Tenured Scientist Executive Committee - August 1998 - October 2001, Chair -

October 2000 - October 2001

Retirement Committee - August 2000 - January 2004

Information Technology Advisory Committee - Chair - January 2001 - present

RELEVANT EDUCATIONAL PROGRAM ACTIVITIES:

Advisor for Joint Program Student: R. Greaves (Graduated 1999)

Examination Committee Member for: L. Souza (MIT - Graduated 2005)

Supervised paper for: C. Williams (MIT-WHOI JP)

12.712 Advanced Marine Seismology, Fall 1984 (with T. Brocher), Spring 1989 (with P. Shaw),

Fall 1991, Fall 1992 and Spring 1995 (with R. Detrick), Spring 1997, Spring 2000

12.571 Seismology Seminar: Numerical Wave Propagation, Fall 2000 (with N. Toksoz and V.

Cormier)

RELEVANT SABBATICAL LEAVE:

Earthquake Research Institute, University of Tokyo, October 2002 to March 2003

RELEVANT PUBLICATIONS:

*Bradley, C.R., Stephen, R.A., Dorman, L.M. and Orcutt, J.A., 1997. Very low-frequency (0.2-

10.0Hz) seismoacoustic noise below the seafloor. J.geophys.Res., 102, 11,703-11,718.

*Dougherty, M.E., Vincent, R.J., Swift, S.A. and Stephen, R.A., 1995. Anisotropic seismic

scattering in old Atlantic crust at Ocean Drilling Program Site 418A. J.geophys.Res.,

100, 10,095-10,106.

*Greaves, R.J. and Stephen, R.A., in press. The influence of large-scale seafloor slope and

average bottom velocity on low-grazing-angle monostatic acoustic reverberation. J.

acoust. Soc. Am.,

Stephen, R.A., 1977. Synthetic seismograms for the case of the receiver within the reflectivity

zone. Geophys. J. R. astr. Soc., 51, 169-181.

Stephen, R.A., Louden, K.E., and Matthews, D.H., 1980. The Oblique Seismic Experiment on

DSDP Leg 52. Geophys. J.R. astr. Soc., 60, 289-300.

Stephen, R.A., 1983. A comparison of finite difference and reflectivity seismograms for marine

models. Geophys. J. R. astr. Soc., 72, 39-57.

Stephen, R.A., 1988b. A review of finite difference methods for seismo-acoustic problems at the

sea floor. Reviews of Geophysics, 26, 445-458.

Stephen, R.A., 1990. Solutions to range-dependent benchmark problems by the finite difference

method. J. Acoust. Soc. Am., 87, 1527-1534.

Stephen, R.A., Koelsch, D., Berteaux, H., Bocconcelli, A., Bolmer, S., Cretin, J., Etourmy, N.,

Fabre, A., Goldsborough, R., Gould, M., Kery, S., Laurent, J., Omnes, G., Peal, K., Swift,

S., Turpening, R. and Zani, C., 1994. The Seafloor Borehole Array Seismic System

(SEABASS) and VLF ambient noise. Marine Geophysical Researches, 16, p. 243-286.

Stephen, R.A. and Swift, S.A., 1994. Modeling seafloor geoacoustic interaction with the

numerical scattering chamber. J.acoust. Soc. Am., 96, 973-990.

Stephen, R.A. and Swift, S.A., 1994. Finite difference modeling of geoacoustic interaction at

anelastic seafloors. J.acoust. Soc. Am., 95, 60-70.

Stephen, R.A., 1996. Modeling sea surface scattering by the finite difference method.

J.acoust.Soc.Am., 100, 2070-2078.

Stephen, R.A., 2000. Optimum and standard beam widths for numerical modeling of interface

scattering problems. J. acoust. Soc. Am., 107, 1095-1102.

Stephen, R.A., Kasahara, J., Acton, G.D. et al., 2003. Proc. ODP, Init. Repts., 200, [CD-ROM].

Available from: Ocean Drilling Program, Texas A&M University, College Station, TX

* - Graduate Student, Summer Student Fellow, or Student Employee under my supervision

Charles Geoffrey Wheathttp://www.sfos.uaf.edu/directory/faculty/wheat/

Mailing Address: Home Address:P.O. Box 475 17753 Northwood PlaceMoss Landing, CA 95039 Prundale, CA 93907Voice (831) 633-7033 e-mail wheat@mbari.org

Education:1986-90 Ph.D. (Oceanography), University of Washington .1983-86 M.S. (Oceanography), University of Washington.1979-83 B.S. (Mathematics), University of New Hampshire.

Honors:1983-84 Egtvedt Scholarship1983 David Drew Award1982 Phi Beta Kappa Honor Society

Professional Experience:2004- Research Professor University of Alaska Fairbanks1999- Adjunct Scientist Monterey Bay Aquarium Research Institute1995- Affiliate Graduate Faculty University of Hawaii1994- Regional Coordinator West Coast and Polar Regions

Undersea Research Center (NURP)1999-2004 Research Associate Professor University of Alaska Fairbanks1999 Visiting Professor Université Paul Sabatier, Toulouse, France1994-99 Research Assistant Professor University of Alaska Fairbanks1993-95 Research Assistant Professor University of Hawaii1993-95 Marine Coordinator (SOEST) University of Hawaii1991-93 Post-Doctoral Fellow University of Hawaii

Professional Societies:American Geophysical Union American Institute of ChemistsNational Ground Water Association Oceanography Society

Research Interests:Use chemical tracers to understand water-rock reactions in different physical, geochemical, andbiological settings, examine effects of fluid flow on diagenetic processes and develop transport-reaction models for these geochemical processes, determine mechanisms of diagenetic reactions,evaluate geochemical cycles and crustal evolution, and conceive experimental approaches to solvegeochemical problems.

Peer-Reviewed Publication:In the last three years I have 17 peer-reviewed publications of which seven were first authored. Ihave published over 50 peer-reviewed manuscripts.

Scientific Expeditions: I have participated in forty-seven cruises, three of which involved the deep ocean drilling (ODPLegs 139 and 168 and IODP Leg 301) and twenty-seven of which included a submersible component.

Five Publications Most Closely Related to This Project:

Wheat, C. G. and M. J. Mottl. 2004. Chapter 19: Geochemical Fluxes Through Ridge Flanks, In,Hydrolgeology of the Oceanic Lithosphere, Ed. E. E. Davis and H. Elderfield, 627-658.

Wheat, C.G., H.W. Jannasch, M. Kastner, J.N. Plant, E.H. DeCarlo, and G. Lebon. 2004. VentingFormation Fluids from Deep Sea Boreholes in a Ridge Flank Setting: ODP Sites 1025 and1026. Geochem. Geophys. Geosyst., 5 (8), Q08007, doi:10.1029/2004GC000710.

Wheat, C.G., H.W. Jannasch, M. Kastner, J.N. Plant, and E.H. DeCarlo. 2003. Seawater Transportand reaction in upper oceanic basaltic basement: Chemical data from continuous monitoringof sealed boreholes in a mid-ocean ridge flank environment. Earth Planet. Sci. Lett., 216,549-564.

Wheat, C. G., H. W. Jannasch, J. N. Plant, C. L. Moyer, F. J. Sansone, and G. M. McMurtry. 2000.Continuous sampling of hydrothermal fluids from Loihi Seamount after the 1996 event. J.Geophys. Res., 105, 19,353-19,368.

Wheat, C. G., M. J. Mottl, A. J. Fisher, D. Kadko, E. E. Davis, E. Baker. 2004. Heat Flow Througha Basaltic Outcrop on a Sedimented Young Ridge Flank. Geochem. Geophys. Geosyst., 5,Q12006, doi: 10.1029/2004GC000700..

Five Other Significant Publications:Wheat, C. G., M. J. Mottl, and M. Rudniki. 2002. Trace Element and REE Composition of a Low-

Temperature Ridge Flank Hydrothermal Spring. Geochim. Cosmochim. Acta. 66, 3693-3705.Wheat, C.G., J. McManus, M.J. Mottl, and E. Giambalvo. 2003. Oceanic Phosphorus Imbalance:

The Magnitude of the Ridge-Flank Hydrothermal Sink. Geophys. Res. Lett., 30(17), 1895,doi: 10.1029/2003GL017318, 2003.

Wheat, C. G., and M. J. Mottl. 2000. Composition of pore and spring waters from Baby Bare:Global implications of geochemical fluxes from a ridge flank hydrothermal system. Geochim.Cosmochim. Acta., 64, 629-642.

Wheat, C. G., H. Elderfield, M. J. Mottl, and C. Monnin. 2000. Chemical composition of basementfluids within an oceanic ridge flank: Implications for along-strike and across-strikehydrothermal circulation. J. Geophys. Res., 105, 13437-13,447.

Jannasch H. W., C. G. Wheat, J. Plant, M. Kastner, and D. Stakes. 2004. Continuous chemicalmonitoring with osmotically pumped water samplers: OsmoSampler design and applications.Limnol. Oceanogr.: Methods, 2, 102-113.

Other Scientific Collaborators Over the Past Four YearsR. Zierenberg (UC Davis); J. Seewald (WHOI); E. Davis (PGC, Canada); A. Fisher (UCSC); M. Lilley(U WA); D. Kelley (U WA); J. McManus (Oregon State U); D. Clague (MBARI); B. Embley(NOAA); M. Tivey (WHOI)

Graduate Advisor: Russell E. McDuff (U WA) Postdoctoral Advisor: Michael J. Mottl (U HI)

Synergistic Activities:A combination of my work and A. Fisher’s work on ridge flank hydrothermal systems provides thefoundation for a graduate level course “Topics in Hydrogeology” at UCSC. Hans Jannasch and I aredeveloping a variety of continuous water samplers. We have developed samplers for high and lowtemperature hydrothermal systems. Modifications to the sampler are now being tested in rivers andestuaries. I have been involved in the NSF’s Research Experience for Undergraduates, MBARI’sSummer Intern, and MATE’s Intern Program, all of which included women and minority students. Iam on the Research Activities Panel for the Monterey Bay NMS and have three graduate students.