RESULTS

Site U1325

Site U1325 (prospectus Site CAS-02C) is located near the southwestern end of the margin-perpendicular transect established during Expedition 311 and is within a major slope basin that developed eastward of the deformation front behind a steep ridge of accreted sediments (Fig. F4). Bathymetry data show that the seafloor in the western part of this slope basin is relatively flat with water depths of ~2200 m. Around Site U1325 the seafloor becomes gradually shallower before it rises rapidly to the east to form the plateau of the second main accreted ridge at water depths of ~1200 m, on which Sites U1327 and 889 are located. A BSR is clearly visible in the eastern part of the slope basin (Fig. F7), but it fades to the west (common depth points [CDPs] 1180–1280 along MCS Line 89-08). The BSR also shows the typical frequency-dependent reflection strength pattern (Chapman et al., 2002) as observed at all other sites. At Site U1325 the BSR is less strong than at the core of a buried ridge of accreted sediments, which is located ~700 m west of this site. The BSR appears to be at ~230 on seismic traveltime-depth conversion, using an average P-wave velocity of 1636 m/s. This average velocity was determined at Site 889 to match observed traveltime depths of the BSR and VSP data (MacKay et al., 1994). We acknowledge that this velocity may not be appropriate in this setting. However, lack of good control in seismic interval velocities from MCS semblance analyses of Lines 89-08 and PGC9902_ODP7 prohibited accurate depth migration.

The primary research objectives for this site are linked to the transect-concept of this expedition. The objectives include

The slope basin is expected to show a different geochemical regime and related geophysical properties than the uplifted ridges of accreted sediments. A summary of major logging and core data is shown in comparison with two key seismic data sets (coincident but of different seismic frequency) in Figures F8 and F9.

Four holes were occupied at Site U1325. Hole U1325A was dedicated for the LWD/MWD program to a total depth (TD) of 300 mbsf (Table T1). Hole U1325B was spudded with the advanced piston corer (APC) system, but problems arose due to thick sand accumulation, causing a switch to the extended core barrel (XCB) for one core section and a switch back to APC. The hole was then advanced by combination of APC, XCB, and pressure coring to 206.5 mbsf. Interspersed with the XCB cores was a Davis-Villinger Temperature Probe (DVTP) run at 140.5 mbsf, which yielded high-quality temperature data. Five pressure cores were deployed in Hole U1325B, but all attempts failed to retrieve sediments under pressure. The last run with the PCS resulted in a stuck tool, which led to the abandonment of the hole. Hole U1325C was drilled to 188 mbsf, where core recovery in Hole U1325B began to deteriorate. Coring operations resumed with the XCB system, interspersed with two pressure coring runs (one failed FPC run and one successful run with the PCS) and two DVTP deployments, deepening the hole to a TD of 304.3 mbsf. Because of degrading weather conditions, it was decided that two separate logging runs would be attempted without calipers to reduce the potential risk of damage to the tool strings. The first run included the phasor Dual Induction Tool (DIT) and the Hostile Environment Gamma Ray Sonde (HNGS). The second run included the Dipole Sonic Imager (DSI), the Scintillation Gamma Ray Tool (SGT), and the Temperature/Acceleration/Pressure (TAP) tool. We were only able to lower the first tool string to 259.8 mbsf, 44.5 m shallower than total depth for coring, and the hole was successfully logged followed by some difficulty reentering the drill pipe. The second tool string (sonic without the Formation MicroScanner [FMS]) was deployed and was only able to reach a TD of 185.8 mbsf; the available hole was logged successfully. The repeat pass of the sonic tool string reached 183.0 mbsf. To ensure that a mudline core was obtained at this site, Hole U1325D was established with one APC core only (4.69 m recovery), indicating a seafloor depth of 2193.2 meters below sea level (mbsl; 2204.8 meters below rig floor [mbrf]). Analyses of the pore water showed that the first core in Hole U1325C had missed the mudline by ~3 m.

The sediments cored at Site U1325 are mostly Quaternary in age, based on the examination of diatoms from Holes U1325B and U1325C. The 304.3 m thick sedimentary section cored at Site U1325 was divided into four lithostratigraphic units based on visual inspection of the recovered cores and analysis of smear slides (Fig. F7).

Lithostratigraphic Subunit IA (0–52.50 mbsf in Hole U1325B and 0–4.69 mbsf in Hole U1325D) is characterized by very abundant, thick, coarse-grained sand layers within fine-grained (clay and silty clay) detrital interlayers. The thickness of the sand layers suggests the depositional environment of a distributary channel within the slope basin with mass transport parallel to the uplifted bounding ridges. Sedimentation rate for the upper 129 mbsf of sediments (lithostratigraphic Units I, II, and upper part of Unit III) was estimated at 43 cm/k.y., the highest sedimentation rate calculated for any site occupied during Expedition 311. Lithostratigraphic Subunit IB (24.00–52.23 mbsf in Hole U1325B) is composed of fine-grained (clay to silty clay) detrital sediments with few thin silty/sandy interlayers from turbidites. The occurrence of only marine diatoms suggests that the terrigenious sediment flux was somehow restricted. In addition, the occurrence of abundant bioturbation and sulfide mottles suggests more hemipelagic dominated sedimentation. Mousselike texture related to the presence of gas hydrate is present at depths as shallow as 26 mbsf. The boundary between lithostratigraphic Subunits IA and IB is marked by a seismic horizon (unconformity) that can be traced for ~1.5 km around Site U1325 (Fig. F7). It separates undeformed seafloor-parallel slope sediments from underlying deformed and slightly faulted sediments. It is likely that at Site U1325 we penetrated a fault within lithostratigraphic Unit II near the base of the unit (Fig. F7).

Lithostratigraphic Unit II (52.23–102.30 mbsf in Hole U1325B) is characterized by fine-grained (clay to silty clay) detrital sediments with intervals of silty/sandy interlayers. We interpret the coarser interlayers as turbiditic deposits. Their frequent occurrence might indicate times of active tectonism. The boundary between lithostratigraphic Units I and II is marked by the absence of diatoms, bioturbation, less intense sulfide mottles, and a sharp decrease in the occurrence of sponge spicules. Mousselike texture related to the presence of gas hydrate was also observed in lithostratigraphic Unit II.

Lithostratigraphic Unit III (102.30–189.44 mbsf in Hole U1325B and 188.80–192.08 mbsf in Hole U1325C) is characterized by fine-grained (clay to silty clay) detrital sediments with abundant sponge spicules and diatoms. We interpret this interval as mixed hemipelagic-turbiditic sediments. The presence of authigenic carbonate cement suggests that diagenetic processes are active in lithostratigraphic Unit III. Soupy and mousselike sediment textures related to the presence of gas hydrates are present in lithostratigraphic Unit III within the depth interval from ~120 to ~150 mbsf. The boundary between lithostratigraphic Units III and IV is marked by the sudden decrease in diatoms.

Lithostratigraphic Unit IV (197.40–206.56 mbsf in Hole U1325B and 198.40–304.30 mbsf in Hole U1325C) is characterized by fine-grained (clay to silty clay) detrital sediments with few silty/sandy interlayers from turbiditic deposits. The poor recovery in this unit limits the observation of sedimentary structures; however, the appearance of several coarser-grained layers indicates low-energy turbidity currents.

The stratigraphic section logged at Site U1325 was divided into three "logging units" based on obvious changes in the LWD/MWD and wireline gamma ray, density, electrical resistivity, and acoustic measurements. There is no obvious correlation between the logging units and lithostratigraphic units.

Logging Unit 1 (0–122 mbsf) is characterized by a well-defined gradual increase in density with depth and a corresponding decrease in porosity. This increase in density is matched by a corresponding increase of resistivity with depth, from ~1 m near the seafloor to ~1.5 m at 122 mbsf. The boundary between logging Units 1 and 2 corresponds to the 0.3 Ma age boundary noted in biostratigraphy.

Logging Unit 2 (122–260 mbsf) is characterized by a uniform density that averages ~1.9 g/cm³. In contrast, the resistivity logs in Unit 2 show alternating thin intervals of high and low resistivity, spanning the range 1–15 m. These high and low resistivities likely correspond to intercalated layers that have high and low gas hydrate concentrations, respectively.

Logging Unit 3 (260–350 mbsf) displays a uniform background resistivity (~1 m) and density (~2 g/cm³). The most striking feature of this unit is the presence of several borehole enlargements.

LWD/MWD-derived resistivity-at-the-bit (RAB) images from Hole U1325A suggest that gas hydrates occur concentrated in thin sand layers within the depth interval between 173 and 240 mbsf (logging Unit 2). The LWD/MWD porosity and resistivity logs from Hole U1325A further show that it is a very heterogeneous gas hydrate–bearing section, composed of alternating layers of gas hydrate–saturated sands and clay-rich layers with little to no gas hydrate. This interpretation is in general agreement with the marked freshening of the interstitial waters observed in sampled sand layers.

There appears to be little correlation between the core-derived physical property data and defined lithostratigraphic or logging units. Sediment density and porosity determined from moisture and density (MAD) analyses show a typical sediment compaction trend with depth. Slight deviations in the density and porosity profiles with depth reflect small-scale lithologic variability and generally match the downhole measured LWD/MWD data. Infrared (IR) imaging of the recovered cores was routinely carried out on the catwalk to detect and characterize the nature of gas hydrates in the cores. A large number of IR-imaged cold spots were detected in the cores from Holes U1325B and U1325C and were partially subsampled for focused interstitial water analyses and microbiology studies. In many cases the IR-imaged cold temperature anomalies correlated with layers of high resistivity and low interstitial water salinities and chloride concentrations, which have been shown to be associated with the occurrence of gas hydrate.

Six deployments of temperature tools were attempted at Site U1325, and all six provided usable data. Three APC3 and one DVTP deployment in Hole U1325B as well as two additional DVTP deployments in Hole U1325C occurred during times of relatively low heave and yielded excellent quality data. A linear fit to the points indicates a thermal gradient of 0.060° The temperature data indicate that the base of the methane hydrate stability zone for this site, assuming a hydrostatic pore pressure gradient and seawater salinity, is at 275

Pressure coring tools were deployed seven times at Site U1325, including two PCS cores, two HRC cores, and one FPC core in Hole U1325B. Hole U1325C included one FPC core from above the projected depth of the BSR and a PCS core from well below the estimated depth of the BSR. Pressure coring proved to be extremely difficult at Site U1325; only the deepest PCS deployment (Core 311-U1325C-10P; 256.5 mbsf) successfully recovered core under pressure, which was investigated by a controlled shipboard degassing experiment. All other attempts to deploy pressure cores failed for various reasons, partially due to difficult lithologic conditions (the presence of unconsolidated fine sand) and the potential effect of adverse ship heave conditions. Degassing of Core 311-U1325C-10P yielded 2.07 L of methane gas and may have contained small amounts of gas hydrates (0.4%) or free gas (0.3%) depending where the base of gas hydrate stability (BGHS) is situated (see uncertainty in temperature-derived BGHS above).

A total of 92 interstitial water samples were processed from two holes cored at Site U1325. The salinity and chlorinity profiles at this site appear to indicate an advective transport system with the occurrence of higher than seawater salinity and chlorinity, which likely comes from a deeper source (~36 and 600 mM, respectively). The chlorinity of this fluid is 7.3% above the modern seawater value, more than twice the value of the interglacial maximum ocean value (3.5%). The elevated solute concentration may instead be caused by low-temperature diagenetic reactions in the deeper parts of the basin. The most plausible candidate for such a reaction is alteration of volcanic ash to clay minerals and/or zeolites. In the zone extending from ~70 to 240 mbsf (the BSR is at ~230 sions to fresher values indicating that gas hydrate was present in the cores and dissociated prior to processing the samples. Intense microbial activity at Site U1325 results in sulfate depletion, phosphate and alkalinity production, and significant Ca and Mg depletion in the interstitial waters of the upper 3 mbsf. At this site the sulfate/methane interface (SMI) was placed between 4 and 5 mbsf, based on samples recovered from Hole U1325D.

Organic geochemical studies at Site U1325 included analysis of the composition of volatile hydrocarbons (C₁–C₅) and nonhydrocarbon gases (i.e., O₂ and N₂) from headspace gas samples, void gas samples, and gas samples recovered during the only PCS degassing experiment. With the exception of several samples that contained a large percentage of air, the void gas was almost entirely methane and a small percentage of carbon dioxide (~0.1%–0.5%). Trace quantities of C₂₊ hydrocarbons (<5 ppmv) were present above the seismically inferred BSR (230 mbsf). With greater depth, the concentrations of ethane, propane, and isobutane increased but did not exceed 15 ppmv. The molecular ratios of methane to ethane (C₁/C₂) were the highest observed during Expedition 311. Ratio values from where gas voids were first observed (9.1 mbsf) to the seismically inferred BSR ranged from ~61,000 to ~173,000 and showed no apparent trend with depth.

Microbiological subsampling was routinely conducted on cores recovered from Holes U1325B and U1325C. On each core run, perfluorocarbon tracer (PFT) was continuously metered into the drilling fluid and fluorescent microspheres were deployed to investigate potential drilling fluid contamination of the core. These analyses confirmed that the center of each whole-round sample remains undisturbed for microbiological subsampling. Additional IR images were taken on the cut ends of each microbiological core section to document the thermal warming process of the core before subsampling.

At Site U1325 the pore water chemistry is distinctly different than what was found at other sites during this expedition, in that chlorinity and salinity increase, rather than decrease, with depth. This trend, attributed to a shallow, more saline sourced fluid, is used as evidence for an advection-driven system; it also shows that this part of the basin is likely detached from the more broad-scale fluid-flow regime seen at the other sites.

Seismic data (Fig. F7) suggest that the sediments cored at Site U1325 are similar to those seen in a seafloor-parallel package of sediments on the southwest side of the buried accreted ridge, but they have been deformed and tilted with small offset faults associated with the uplift of the underlying ridge. Enhanced advective fluid flow from the buried accreted basin resulted in gas hydrate formation within the overlying deformed section, preferentially in the coarser-grained turbidite sequences. In contrast, the southwest part of the basin has relatively little deformation and postulated reduced fluid flow and therefore less gas hydrate, which also explains the lack of a strong BSR in that part of the basin.

Although the BSR is not very prominent near Site U1325, the stratigraphic section beneath the projected BSR generally shows high-amplitude reflectors and updip amplitude truncations at the BSR, typical of free gas trapped beneath the BSR. Data from downhole logging and coring also revealed lateral homogeneity between the holes at this site, which is a testament to the orientation of the holes along structural strike in a northwest-southeast direction, avoiding the steep southwest-northeast-dipping slope seen in the seismic data.

Site U1326 (prospectus Site CAS-03C) is located on an uplifted ridge of accreted sediments at the southwest end of the multisite transect established during Expedition 311 (Fig. F5). Recently acquired bathymetry data reveal a collapse structure near the originally proposed primary Site CAS-03B, which may have complicated the recent geologic history of this site. We decided to switch the former alternate location CAS-03C to the primary site to avoid coring directly into the slump feature.

The headwall of the slump feature near prospectus Site CAS-03B is ~250 m high and the slump has eroded a ~2.5 km long section into the ridge. Further examination of the bathymetry data from this area also reveals the occurrence of continuous linear features crossing the ridge in an almost east-west direction. These linear features are clearly associated with faults as seen on Figure F10. The outcrop of these faults at the seafloor generate a surface displacement of up to 25 m and can be seismically traced from the surface down through the sedimentary section to depths below the BSR. The occurrence of these deep throughgoing faults is generally limited to the area of the slump scar. The seismic character of the ridge also changes from the southwest to the northeast across the ridge, with the southwest-facing part of the ridge characterized by strong semicontinuous reflectivity (Figs. F11, F12), while the seismic reflectivity disappears underneath the northeast-facing flank of the ridge. The differences in the seismic character across the ridge cannot be easily explained, and it is one of the research focuses of the site. The BSR is present underneath most of the ridge (Fig. F10), but it is almost absent underneath the slump feature in association with the most heavily faulted sediments.

The objectives of coring and logging at this site are tied to completing the transect of scientific research holes across the northern Cascadia margin. Site U1326 is the closest location to the deformation front, and it probably represents the tectonically youngest occurrence of gas hydrate on the northern Cascadia margin; as such, our primary research objectives include

The operational plan to achieve these objectives was based on a general three-hole concept, which included an LWD/MWD logging hole, a continuous core hole to characterize geochemical and microbiological baselines and proxies for the occurrence gas hydrate, and an additional "tool" hole for specialized pressure coring and selected spot-coring using conventional systems. The special tools hole was also intended to be logged with the conventional IODP wireline logging tool strings.

After transiting from Site U1325, the LWD/MWD bottom-hole assembly (BHA) was tripped to the seafloor. Hole U1326A was spudded at 1445 h on 22 September 2005 at an estimated seafloor tag depth of 1828.1 mbsl (1839.0 mbrf). To avoid blowing out the top of the hole, we adopted a controlled-spud program that featured reduced drilling fluid circulation rates of only 100 gpm and a bit rotation rate of 10–15 rpm. As the hole was advanced, both the circulation rate and bit rotation rate were increased to maintain a 50 m/h rate of penetration. The LWD/MWD safety protocol was followed without incident and required no corrective action. The hole was drilled to a TD of 300 mbsf; the drill string was pulled clear of the seafloor at 0600 h on 23 September. Hole U1326B was spudded 15 m northeast of Hole U1326A at 1205 h on 23 October, but the first core failed to establish the depth of the mudline and it was decided to start a new hole. Without offsetting from the location of Hole U1326B, Hole U1326C was spudded at 1245 h on 23 October. The first core established a seafloor depth of 1828.0 mbsl (1839.6 mbrf). On the fourth APC core (~30 mbsf), we unexpectedly hit APC refusal and switched to XCB coring. Hole U1326C was advanced by XCB coring to 82.7 mbsf (Table T1), which was followed by three consecutive pressure core deployments within a high–electrical resistivity zone identified on LWD/MWD downhole logs. In this case, the FPC and HRC pressure core runs were added to the traditional continuous core hole to increase the total number of pressure core runs at this site. The FPC was the first pressure core system deployed at this site; it recovered a partial core (15 cm) at less than full pressure. The second system to be deployed was the PCS, which recovered a partial core under pressure. The third pressure core system deployed was the HRC, which was "packed off" with sand, and the cutting shoe and the lower part of the autoclave was unscrewed and left behind in the hole, resulting in the termination of Hole U1326C at a TD of 86.7 mbsf. After tripping the BHA back to the seafloor, the ship was moved ~30 m southwest (15 m from Hole U1326A). Hole U1326D was spudded at 1130 h on 24 October and drilled to 78.8 mbsf in preparation for continued coring to a target depth of 300 mbsf. Because of problems associated with the heave state and schedule limitations, all pressure coring operations were suspended for the remainder of the hole. XCB coring deepened the hole to 271.4 mbsf. With the forecast of deteriorating weather conditions on the morning of 26 October, it was decided to stop coring and complete the hole by drilling to 300 mbsf. Despite the marginal conditions, we did attempt three deployments with the DVTP (252.2, 271.4, and 300 mbsf), which yielded degraded data. After completing coring and drilling operations, we then decided to conduct a single downhole logging run with a nonstandard IODP tool string, which included the SGT, DIT, and the DSI. At 2315 h on 26 October, the logging tool string was lowered to 298.4 mbsf; two successful logging passes were made, with the tool string back on deck at 0345 h. The drill string was pulled clear of the seafloor at 0530 h on 27 October, ending operations in Hole U1326D.

The 271.40 m thick Quaternary sedimentary section cored at Site U1326 was divided into three lithostratigraphic units (Fig. F13). Lithostratigraphic Unit I (0–1.50 mbsf in Hole U1326B and 0–24.13 mbsf in Hole U1326C) is characterized by fine-grained (clay to silty clay) detrital sediments with thin silty/sandy interlayered turbidite sequences. Foraminifers, shell fragments, sponge spicule remains, mottling, and bioturbation, together with the high marine versus nonmarine ratio of diatoms, indicate hemipelagic sedimentation mixed with turbiditic inputs (coarse-grained facies). Authigenic carbonate cement is also present in lithostratigraphic Unit I.

Lithostratigraphic Unit II (24.13–82.70 mbsf in Hole U1326C and 88.40–146.30 mbsf in Hole U1326D) is also dominated by fine-grained (clay to silty clay) detrital sediments with intervals of turbidite deposited silty/sandy interlayers, but diatoms are absent and other biogenic components are rare. The frequent occurrence of turbidites might indicate times of active tectonism. Below 30.4 mbsf, abundant soft-sediment deformation and dipping strata show that tectonism is more active at the westernmost end of the transect drilled during this expedition. Authigenic carbonate cement and a carbonate concretion also are present in lithostratigraphic Unit II. Soupy and mousselike textures indicative of gas hydrate occurrence were observed throughout this unit. The lithostratigraphic Unit II/III boundary is marked by the appearance of diatoms, although their abundance is low.

Lithostratigraphic Unit III (146.30–271.40 mbsf in Hole U1326C) is characterized by fine-grained (clay to silty clay) detrital sediments with few thin silty/sandy turbidite interlayers. We interpret this interval as mixed hemipelagic-turbiditic deposition. Soupy sediment textures related to the presence of gas hydrate are also present in lithostratigraphic Unit III.

Precoring LWD/MWD logging was conducted at Site U1326 to direct special tool deployments, such as the PCS, HRC, and FPC pressure cores. The stratigraphic section logged at Site U1326 was divided into three "logging units" based on obvious changes in LWD and wireline gamma ray, density, electrical resistivity, and acoustic measurements. The three identified logging units do not correspond to the defined lithostratigraphic units.

Logging Unit 1 (0–72 mbsf in Hole U1326A) is characterized by a resistivity trend that steadily increases from ~1 m near the seafloor to ~1.5 m at the bottom of the unit. This increase in resistivity with depth is matched by an increase in density. This unit shows only a few small resistivity "spikes" (e.g., at ~52 and 60 mbsf in the LWD logs) that may be attributed to gas hydrates.

Logging Unit 2 (72–240 mbsf in Hole U1326A) is characterized by uniform density with depth and includes a prominent high-resistivity section from 72 to 107 mbsf in Hole U1326A, with peaks >40 m. This interval of high resistivity also includes a number of alternating thin intervals of very low resistivities. These high and low resistivities likely correspond to intercalated layers that have high and low gas hydrate concentrations, respectively. The P-wave velocities measured by wireline logging in Hole U1326D show highly variable values (between 1750 and >3000 m/s) in the same high-resistivity interval. The high values of P-wave velocity are consistent with high concentrations of gas hydrate.

The top of logging Unit 3 (240–300 mbsf in Hole U1326A) is marked by an increase in density, which remains constant to 300 mbsf. The background resistivity also increases slightly and displays a clear peak, reaching 5 m in the interval 255–261 mbsf. This resistivity peak could be due to gas hydrate or free gas. Free gas seems more likely, as this interval is located below the BSR depth at this site, estimated from seismic reflection data at 234 mbsf. On the other hand, P-wave velocities are at least 1700 m/s in this unit and there is no sign of the low velocities as expected in a free gas zone.

LWD/MWD-derived RAB images from Hole U1326A also indicate the presence of gas hydrate in the high-resistivity interval observed in logging Unit 2, with gas hydrate–rich layers alternating with low-resistivity layers that likely contain little or no gas hydrate (Fig. F13). When the RAB images are examined in greater detail, they also show apparent stratigraphic layers in the interval from 50 to 300 mbsf, uniformly dipping to the north-northeast with dips between 45° and 85°. This is in agreement with the west-northwest–east-southeast strike of the uplifted ridge penetrated by Hole U1326A.

The Archie interpretation of water saturations from electrical resistivity logging data yielded evidence for relatively shallow gas hydrate occurrences at this site within the depth interval from ~50 to 100 mbsf, with inferred water saturations as low as 20% (Fig. F13). This interpretation is in general agreement with the freshening of the pore waters observed in sand layers at Site U1326. The IR core images taken on the catwalk reveal cold anomalies due to gas hydrate dissociation, which give an independent map of gas hydrate occurrence and concentrations. In some cases IR-imaged cold temperature anomalies correlate with layers of high resistivity. In other cases, however, cold intervals in the IR images are harder to correlate to high-resistivity peaks in the wireline or LWD/MWD logs because of incomplete core recovery and intrasite geologic variability.

Cold temperature anomalies were observed at a wide range of depths from 70 to 250 mbsf, and catwalk sampling was conducted based on these scans. Many interstitial water samples were taken based on IR data to extend the chlorinity anomaly database available for calibrating IR data as a proxy for gas hydrate saturation. We note that the maximum depth of observed IR anomalies is deeper than the anticipated BSR depth of 230 mbsf. It was also suggested that the chlorinity anomaly associated with gas hydrate may actually extend to a depth as great as 270 mbsf at this site. This apparent conflict between the depth of the BSR and the observed occurrence of gas hydrate can be explored with closer examination of gas hydrate stability condition at this site. Because of difficult weather conditions throughout the duration of the coring operations at this site, we deployed only four temperature tools. For the most part, all of the data from the temperature tool deployments were degraded to some extent. At this time we have extrapolated the temperature data from Site U1325 to estimate temperature conditions at Site U1326. With a seafloor temperature of ~3.03C and a geothermal gradient of ~60C/km, the depth to the base of the methane hydrate stability zone was estimated at Site U1326 to ~250 mbsf. A predicted methane hydrate stability zone depth of 250 mbsf would help explain most of the deeper IR and chlorinity inferred gas hydrate occurrences, but the several isolated anomalies below this depth require further postcruise consideration.

At Site U1326, only one PCS core (Core 311-U1326C-12P) was recovered successfully under pressure and investigated by controlled shipboard degassing experiments. This core was taken at 84.2 mbsf. The degassing of this single PCS core yielded 19.1 L of gas, which was determined to be equivalent to a pore space gas hydrate saturation of 40%, which is in close agreement with the gas hydrate saturations estimated from the LWD/MWD Archie resistivity calculations in the same interval.

This site was selected to further characterize the occurrence of what could be the tectonically youngest gas hydrate occurrence on the Northern Cascadia margin, considering its location within the westernmost portion of the deformation front. Hydrocarbon headspace gas measurements from Holes U1326C and U1326D show that methane is the dominant hydrocarbon gas within the cored interval at this site. Although the C₂₊ hydrocarbon void gas concentrations were <125 ppmv for all samples, their relative abundances and distribution were valuable for describing the gas hydrate system at Site U1326. Low C₁/C₂ ratios within the interval from ~35 to ~72 mbsf were determined to be directly associated with two recovered gas hydrate samples. With greater depth, ethane concentrations returned to the near-surface concentrations close to the depth of the seismically inferred BSR. Isobutane concentrations were also elevated within the same interval, which may indicate the presence of a Structure II gas hydrate. The occurrence of more complex hydrocarbon gases generally indicates contribution of a deeper gas source. The salinity and chlorinity profiles at this site also point to a deeper fluid source with a chloride concentration higher than seawater, indicative of low-temperature diagenetic reactions in the deeper parts of the site. Except for the difficulties experienced with pressure coring and special temperature tool deployments, all of the objectives set for Site U1326 were considered fulfilled.

Site U1327 (prospectus Site CAS-01B) is located near Sites 889/890, approximately at the midslope of the accretionary prism over a clearly defined BSR estimated to be at 223 mbsf (Fig. F14, F15). The primary research objectives for this site are linked to the transect concept of this expedition. Sites 889/890 provided critical baseline data for the development of the objectives of this research expedition. Historical work with data from Sites 889/890 has shown that the concentration of gas hydrate in sediments has been estimated by using (1) deviations in interstitial water chlorinities from measured baseline conditions, (2) electrical resistivity measurements by applying Archie's relation, and (3) both seismic- and downhole logging-derived P- and S-wave velocities. But results from Leg 146 left many questions unanswered (Riedel et al., 2005), such as:

Answers to these questions are needed to calibrate remote sensing techniques, such as reflection seismic and CSEM surveys, which can be obtained through research coring and downhole logging.

Five holes were occupied at Site U1327 (Table T1). Hole U1327A was dedicated to LWD/MWD measurements to a TD of 300 mbsf. Initially we planned to drill to 350 mbsf, but tight time constraints during LWD/MWD operations made it necessary to reduce the depth of the planned penetration at this site. The first APC core in Hole U1327B missed the mudline with a full core, the core was curated, and a new hole was spudded without offsetting the ship. Hole U1327C was then cored (10 APC cores, 22 XCB cores, and 3 PCS cores; recovery = 88.3%) to 300.0 mbsf. The PCS was deployed three times in Hole U1327C, and four advanced piston corer temperature (APCT) tool measurements were made (Cores 311-U1327C-3H, 5H, 7H, and 9H). Three additional deployments using the DVTP and Davis-Villinger Temperature-Pressure Probe (DVTPP) were attempted, but data quality is marginal due to strong heave conditions and instrument failures. In Hole U1327D, which was drilled and cored as a special tools hole, two APC cores were also taken from the surface to 16.4 mbsf for a high-resolution microbiological and geochemical study of the SMI. In this hole, the PCS was deployed three times, together with four deployments of the HRC and two deployments of the FPC system. The last pressure core was taken at 246.5 mbsf, and the hole was advanced to a TD of 300 mbsf for the logging program.

The first tool string deployed was the triple combination (triple combo), which reached 295.4 mbsf, and the hole was logged to near the top of the logging run without incident. A combination of a ship heave event (>3 m) and the oversized borehole apparently caught and tore off the density tool caliper arm. The damaged tool string was returned to the ship without further incident. The VSP logging program in Hole U1327D was started the following morning with the 1 h long preshooting marine-mammal observation period and a 30 min pressure ramp-up time for the generator-injector gun. The VSP program was successfully carried out with 16 clamping stations covering the depth range from 181 to 276 mbsf before the arm on the Well Seismic Tool (WST) apparently broke. The WST was returned with some difficulties to the ship. Because of the critical nature of the acoustic wireline logging program to the expedition, it was decided to drill a new hole and acquire additional pressure cores and a wireline acoustic logging survey.

Hole U1327E was advanced to 3 mbsf, and a single 9.5 m long APC core was taken for high-resolution microbiological and geochemical sampling of the SMI, which was partially missed during an earlier attempt. Two additional PCS cores and one HRC core were taken, out of which only the second PCS at ~80.5 mbsf recovered sediment under pressure. Excessive heave >3.5 m forced the termination of pressure coring operations, and the hole was advanced by drilling to a completion depth of 300 mbsf to prepare for the second wireline logging run. Because of the excessive heave conditions it was decided to run a nonstandard tool string composed of the HNGS-DIT-DSI, which allowed measurement of natural gamma, resistivity, and acoustic data (V_P and V_S). Two successful runs of this tool string were completed, recovering high-quality downhole logging data.

Site U1327 is located near two prominent topographic highs, composed almost entirely of accreted sediments that rise >200 m above the surrounding seafloor (Fig. F14). The ridges of accreted sediment lack any coherent seismic reflections and are associated with underlying thrust faults that contributed to the overall uplift of the area between the two ridges (Westbrook, Carson, Musgrave, et al., 1994; Riedel, 2001). Site U1327 is situated near the northwest flank of the easternmost ridge and is characterized by a ~90 m thick cover of slope-basin sediments, underlain by a thick section of accreted sediments (Fig. F15). The stratigraphy at Site U1327 was divided into three lithostratigraphic units (Fig. F16).

Lithostratigraphic Unit I (0–90.1 mbsf in Hole U1327C; age = Holocene–Pleistocene; <0.3 Ma) is composed of dark greenish gray and dark gray clay and silty clay, often interbedded with silt, clayey silt, sandy silt, sand, and gravel layers. Lithostratigraphic Unit I is characterized by fine-grained detrital sediments (clay and silty clay) with abundant coarse-grained layers up to 6 cm thick indicating turbiditic deposits and a sedimentation rate of 22 cm/k.y. Authigenic carbonate cement is present in Unit I, but no evidence for dolomite precipitation is found, which is inferred from interstitial water analyses. A unique characteristic of Unit I is the anomalous occurrence of lithified carbonate nodules and rocks of various lithologies, such as granite, which probably are dropstones from rafting icebergs. The lithostratigraphic boundary between Units I and II is marked by a sharp decrease in sand and silt layers and the onset of diatom-rich sediments. It is also the seismically inferred boundary between slope-basin type and accreted sediments (Fig. F15).

Lithostratigraphic Unit II (90.1–170.4 mbsf in Hole U1327C; age = Pleistocene; >0.3–1.0 Ma) is composed of dark greenish gray and dark gray clay, clay with diatoms, and silty clay, silty clay with diatoms, and diatom silty clay locally interbedded with sandy silt and sand layers and lenses. Very few carbonate cements are present in Unit II, but lithified carbonate nodules and exotic rocks (some up to 8 cm in diameter) as described in Unit I are very abundant. Within Unit II soupy and mousselike sediment textures related to the presence of observed gas hydrate can be correlated to IR-imaged cold spot anomalies detected on the catwalk. The sedimentation rate of Unit II is estimated at ~16 cm/k.y., and the intervals with a high ratio of nonmarine versus marine diatoms indicate the increasing contribution of terrigeneous detrital sediments from land sources via turbidites. The great abundance of marine diatoms along with resting spores within lithostratigraphic Unit II suggest blooming in shallow-water shelf environment and coastal upwelling then reworking by turbidity currents.

Lithostratigraphic Unit III (170.4–TD in Hole U1327C; age = Pleistocene; >1 Ma) is composed of dark greenish gray and dark gray silty clay in the upper part of the unit, whereas the lower part (below 248 mbsf) is dark greenish gray silty clay with diatoms. Lithostratigraphic Unit III is distinguished from lithostratigraphic Unit II by the sudden absence of diatoms, as well as the degree of induration of the sediments. Diatoms reappear at the bottom of Unit III. Few carbonate cements are present and lithified carbonate nodules and exotic rock clasts were found, especially within Core 311-U1327C-24P taken at 197.3 mbsf. The depositional environment for Unit III was interpreted as an abyssal plain with sediment transport and deposition dominated by low-energy turbidity currents. The sedimentation rate in this section, as determined from biostratigraphic analyses of diatoms, is low for this site at ~12 cm/k.y., which is consistent with a basin-plain setting.

The downhole logged section at Site U1327 was divided into three "logging units" based on obvious changes in the LWD/MWD and wireline gamma ray, density, electrical resistivity, and acoustic measurements. There is no apparent correlation between the logging units and lithostratigraphic units at this site.

Logging Unit 1 (0–120 mbsf) is characterized by a resistivity trend that steadily increases from ~1 m near the seafloor to ~2 m at the bottom of the unit. P-wave velocities in this unit average ~1550 m/s.

Logging Unit 2 (120–240 mbsf) is characterized by a constant background resistivity value of ~2 m and relatively high P-wave velocities that average ~1750 m/s over most of the interval. This unit shows a number of thin (0.5–1.0 m thick) high-resistivity sections that may be attributed to gas hydrates, and the occurrence of relatively high downhole measured P-wave velocities in these same intervals also indicates the presence of gas hydrate. A thick section of continuous high electrical resistivities and P-wave velocities combined with low density measurements was observed in the LWD/MWD data at 120–138 mbsf in Hole U1327A, which was the target of several pressure coring deployments (see below for details). However, it was later determined that this high-resistivity zone was laterally discontinuous and was penetrated in the adjacent Holes U1327C and U1327D at a much greater depth (ranging from 20 to 35 m deeper) and was not intersected in Hole U1327E.

The top of logging Unit 3 (240–300 mbsf) is defined by a sharp decrease in P-wave velocity. Below 240 mbsf, P-wave velocities drop to very low values near fluid velocities (~1500 m/s), suggesting the presence of small amounts of free gas. Logging Unit 3 also displays a small drop in resistivity compared to logging Unit 2. Although resistivity tends to be just above 2 m in Unit 2, it is just below 2 m in Unit 3.

Variations in the core-derived physical properties apparently do not correlate well with the identified lithostratigraphic and logging units, with the exception of the boundary between lithostratigraphic Units I and II, marked by a sharp increase in magnetic susceptibility. Sediment density and porosity determined from MAD analyses show a typical trend with depth, suggesting normal compaction. Slight deviations from this trend reflect small-scale lithologic variability and generally match the porosity and density trend determined from the LWD/MWD data.

Infrared imaging of the recovered cores was routinely carried out on the catwalk to detect and characterize the nature of gas hydrates in the cores. A large number of IR-identified cold spots were detected in the cores from Holes U1327C and U1327D; however, an apparent depth mismatch in the occurrence of major cold core sections between the holes indicated significant intrasite geologic variability. Apparent mismatches between the IR-inferred gas hydrate occurrences in Hole U1327C and the LWD/MWD resistivity–inferred gas hydrate occurrences in Hole U1327A further document the lack of lateral continuity at this site. In situ temperature measurements with the APCT (four measurements), DVTP (one deployment, instrument failure), and DVTPP3 (two deployments, poor quality due to heave and instrument calibration problems) were conducted. The data suggest a geothermal gradient of ~61°C/km, which is considerably higher than what was estimated for Site 889 (~54°C/km).

The PCS was deployed eight times at Site U1327 (three times in Hole U1327C, three times in Hole U1327D, and twice in Hole U1327E), five of which recovered sediment under pressure. In addition to the PCS deployment, the HRC was used four times (with three cores recovered under pressure) and the FPC was used twice, but only one of the FPC cores was recovered under pressure. Degassing of the five PCS cores from this site that were recovered under pressure showed variable gas concentrations with depth. The deepest PCS core was taken at 246.5 mbsf, which is ~25 m deeper than the seismically inferred BSR depth. This pressure core (Core 311-U1327D-17P) had a pore space methane concentration of 208 mM, which is equivalent to a free gas concentration in the pore space of the sediment of 0.9%. The other four PCS cores were taken from within the predicted depth interval of the methane hydrate stability zone. Core 311-U1327E-3P is the shallowest PCS core taken at this site, from ~80.5 mbsf. It yielded 1.31 L of methane (81 mM) or, equivalently, 0.2% gas hydrate concentration. The remaining three PCS cores were taken at 122.3, 155.6, and 197.8 mbsf (Core 311-U1327C-15P yielded 1.1 L [94 mM] of methane; Core 311-U1327D-10P yielded 9.4 L [673 mM] of methane; and Core 311-U1327C-24P yielded 4.0 L [251 mM] of methane). Of these three cores, only Core 311-U1327D-10P yielded enough gas to infer the occurrence of a significant amount of gas hydrate, with an estimated gas hydrate pore space concentration of ~8%. The other two PCS cores yielded gas hydrate pore space concentrations ranging from 0.2% to 1.8%.

Three HRC cores (Cores 311-U1327D-4E at 125.3 mbsf, 311-U1327D-12E at 170.5 mbsf, and 311-U1327D-14E at 217.7 mbsf) and one FPC core (Core 311-U1327D-13Y at 203.6 mbsf) were successfully recovered and transferred under pressure to storage chambers for shore-based analyses. All of these cores were imaged with X-ray and logged for P-wave velocity and density within their storage vessels. Some of the recovered pressure cores exhibited evidence of gas hydrate, including high P-wave velocities and anomalous low density readings.

High-resolution interstitial water sampling was carried out to characterize the SMI, which was determined to be located between 9 and 10 mbsf. An overall smooth decreasing trend in pore water chlorinity and salinity is observed, similar to results from Sites 889/890 (Westbrook, Carson, Musgrave, et al., 1994). At ~120 mbsf the chlorinity and salinity profiles exhibit distinct anomalies that likely indicate freshening as a result of the dissociation of gas hydrate during the core recovery process (Fig. F16). Chloride values as low as 70 mM (equivalent salinity = 3.7) were measured in two samples, correlated to sand layers (up to 3 cm thick) that also showed clear IR cold spot anomalies. Such a low pore water chlorinity is equivalent to a pore space gas hydrate concentration of ~80%. No chlorinity anomalies occur below ~225 mbsf, which is close to the seismically inferred depth of the BSR. However, the strongly decreasing chlorinity profile from the surface to below the BSR at Site U1327 suggests mixing of standard marine pore water with a deep-sourced, relatively fresh fluid. Interestingly, interstitial water chlorinity and salinity remain almost constant beneath the BSR.

Organic geochemical studies at Site U1327 included analysis of the composition of volatile hydrocarbons (C₁–C₅) and nonhydrocarbon (i.e., O₂ and N₂) gases from headspace gas samples, void gas samples, and gas samples recovered during PCS degassing experiments. The predominant hydrocarbon gas found in the cores from Site U1327 was methane; however, we did see an increase in ethane concentrations in the void and headspace gases collected from the stratigraphic section overlying the projected depth of the BSR. This increase in ethane concentrations near the BSR can also be seen in the plot of the C₁/C₂ void gas ratios (Fig. F16), which decrease with depth toward the BSR. Other studies have shown that void gas ratios can decrease in a gas hydrate with the preferential selection of ethane into the gas hydrate structure. But the observed increase in the C₁/C₂ ratio below the projected depth of the BSR may indicate a methane-enriched free gas accumulation. In general, the C₁/C₂ ratios were generally high (>1000), indicating a predominant microbial origin for the observed methane.

Microbiological subsampling was routinely conducted on cores recovered from Hole U1327C. On each core run PFT was continuously metered into the drilling fluid, and fluorescent microspheres were deployed on selected cores to investigate potential drilling fluid contamination of the core. These analyses confirmed that the center of each whole-round sample remains undisturbed for microbiological subsampling. Additional IR images were taken on the cut ends of each microbiological core section to document the thermal warming process of the core before subsampling.

The primary research objectives of this site are linked to the results from Sites 889/890 of Leg 146 to delineate critical geochemical, geophysical, and microbiological data for gas hydrate proxy analyses. Site U1327, along with Sites 889/890, is the center of a research study area that since 1992 has been the focus of many interdisciplinary gas hydrate studies.

Geochemical analyses of recovered gas samples and interstitial fluids documented a relatively complex fluid regime for this site, similar to what was observed at Sites 889/890 and U1329. The rapid chlorinity concentration decrease with depth strongly suggests fluid communication with a deep-seated, fresher fluid source. Earlier interpretations of the chlorinity profile measured at Sites 889/890 attributed the pore water freshening entirely to gas hydrate dissociation upon core recovery (Hyndman et al., 1999). However, the new interstitial water data collected at Site U1327, in combination with other gas hydrate proxy data (such as IR images and downhole logging measurements), strongly support the development of a new undisturbed baseline for interstitial water chlorinity along the Cascadia margin that progressively decreases with depth, similar to what was suggested by Ussler and Paull (2001). In other words, gas hydrate–related pore water freshening at Site U1327 is interpreted to be limited to only the interval from ~120 to ~220 mbsf, which is near the depth of the seismically identified BSR. Geochemical analyses of hydrocarbon gases from this site reveal a similar story as the analysis of the interstitial fluids with the gas chemistry in the inferred gas hydrate–bearing section dominated by gas hydrate formation processes with an apparent increase in the more stable gas hydrate natural gas components.

Identifying gas hydrate and constraining its relative abundance in combination with providing physical models for the BSR are critical geophysical objectives at this site. A suite of geophysical experiments was conducted including precoring LWD/MWD logging, conventional wireline logging, and VSP to characterize the physical properties of gas hydrate–bearing sediments. The presence of gas hydrate is generally characterized by increases in measured electrical resistivity and acoustic velocity. However, the LWD/MWD data from Hole U1327A showed an 18 m thick zone of increased resistivity and acoustic velocity values combined with a decrease in density, which was interpreted to contain large amount of gas hydrate, with concentrations >50% of the pore volume. However, the same interval was penetrated in the adjacent core holes, Hole U1327C and Hole U1327D, at much greater depths and with lower estimated gas hydrate concentrations inferred from the wireline electrical and acoustic logs. In the repeat wireline logging in Hole U1327E, no evidence of this interval was found. This shows large intrasite variability in gas hydrate content that is probably controlled by lithostratigraphic changes or structural complexities. This observation has dramatic implications on the calibration of geophysical surveying techniques such as seismic methods or CSEM surveys that are commonly used to detect and quantify gas hydrates.

The combined use of IR imaging, interstitial pore water analyses, and void/headspace gas sampling revealed that many IR cold spots identified on the catwalk occur in relatively thin but coarser-grained intervals of sand and/or silty sand (interpreted to represent turbidite deposits) with gas hydrate concentrations in several cases exceeding 80% of the pore space. The gas hydrate forms preferentially in these coarser-grained sections. Therefore, it is likely that the 18 m thick LWD/MWD-measured high-resistivity and acoustic velocity interval (120–138 mbsf) in Hole U1327A is a localized feature made up of discontinuous thinly bedded gas hydrate–saturated turbidite sand lenses, that when surveyed with a logging tool with relatively lower vertical resolution the gas hydrate–bearing section appears more massive in nature as a single unit on the downhole log.

The results of the VSP seismic experiment taken in combination with the downhole acoustic logging from Hole U1327E also shows a relatively thick zone below the depth of the BSR that probably contains a considerable amount of free gas. The acoustic velocity decrease at the BSR is not abrupt; it is more transitional across a ~25 m thick interval from >1800 m/s in the gas hydrate stability zone to as low as 1280 m/s in the underlying section. This confirms earlier interpretations of the frequency-dependent reflection behavior of the BSR from vertical incidence seismic data. The BSR was thought to be a gradient zone in which velocity decreases over several meters (Chapman et al., 2002).

This site was intended to characterize the gas hydrate occurrence on the northern Cascadia margin to establish an understanding of the geologic, geophysical, and geochemical controls on the occurrence and abundance of gas hydrates along the five-site transect established during this expedition. All of the objectives set for Site U1327 are considered fulfilled.

Site U1328 (prospectus Site CAS-06A) is located within a seafloor cold vent field, 2 km x 4 km, consisting of at least four vents associated with near-surface faults. The cold vents are characterized by near-vertical seismic blank (or wipeout) zones that are between 80 and several 100 m wide and show a clear east-west trend as identified from 3-D seismic imaging. The most prominent vent in the field, referred to as Bulls-eye vent, is the target of this site and has been the subject of intensive geophysical and geochemical studies since 1999 (e.g., Riedel et al., in press). Site U1328 is different from all of the other sites visited during this expedition in that it represents an area of active, focused fluid flow. A number of seismic surveys cross this site, including two single-channel seismic (SCS) 3-D surveys and a regional MCS data set. In Figure F17 we show MCS Line XL07 and the main lithostratigraphic units, hole locations, and penetration depths at this site.

Several different mechanisms have been proposed for the origin of the seismic blanking observed in the Bulls-eye vent area and for the implications concerning the nature of the fluid venting (Riedel et al., 2002, in press; Zühlsdorff and Spiess, 2004; Wood et al., 2002). The objectives of coring and logging at this location are to test the different models for the cold vent structure and associated causes of seismic blanking, the rate of methane advection, and potential loss of methane into the water column. It was important to obtain a high-resolution temperature profile for this area to assess any evidence of active fluid flow. Pressure coring using the PCS system will help assess the occurrence of free gas within the gas hydrate stability zone below Bulls-eye vent and possibly ascertain the cause of the observed seismic blanking. Additional pressure coring using the HRC and FPC systems will be used to recover high-quality gas hydrate–bearing core for shore-based analyses.

Five holes were occupied at Site U1328. Hole U1328A was dedicated to LWD/MWD measurements to a TD of 300 mbsf. Hole U1328B was continuously cored (six APC, two XCB, and two PCS cores; recovery = 72.8%) to a depth of only 56.6 mbsf and was terminated after strong winds and severe ship heave conditions required us to pull out of the hole. Two APCT measurements were made (APCT and APC3). As a calibration experiment, the DVTPP was also deployed at the bottom of Hole U1328B. After waiting on weather for 16 h, conditions improved to the point to allow drilling and coring operations to continue. Hole U1328C was drilled from the seafloor to the maximum depth of Hole U1328B (56.5 mbsf). Hole U1328C was then continuously cored (4 APC cores, 22 XCB cores, and 1 PCS core; recovery = 80.7%) to a TD of 300 mbsf. In addition, three APCT and two DVTPP temperature measurements were made. Hole U1328C was wireline logged with the triple combo and FMS-sonic tool strings. The triple combo logged from a total depth of 294 mbsf, and two uphole passes of the FMS-sonic tool string logged the same depth interval. The wireline logging program in Hole U1328C included a VSP survey, with the deepest clamping position at 286 mbsf. The VSP included 35 clamping positions, with the uppermost station at 106 mbsf. Hole U1328D was cored as a special high-resolution combined microbiology and geochemistry research hole with two XCB cores and a single FPC core taken at the bottom of the hole. Hole U1328E was a special tools hole, which also included the deployment of six XCB cores within the upper 46.0 mbsf to recover additional samples of gas hydrate. Seven pressure cores were taken (three PCS, two HRC, and two FPC), separated by XCB cores and drilled intervals. Hole U1328E also included two DVTPP deployments for temperature data. In Figures F18 and F19, data from LWD/MWD logging (RAB images, porosity, and Archie-derived pore water saturations), core-derived physical property data (porosity), interstitial water chlorinity, and C₁/C₂ ratios from void gas samples are shown in comparison to the two key crossing seismic lines from this site.

At Site U1328 a 300 m thick sequence of Quaternary (0–1.6 Ma) slope and slope basin sediments was recovered (Fig. F17). The biostratigraphy determined for Site U1328 was based on the examination of diatoms from Holes U1328B and U1328C. The stratigraphic section cored and logged at Site U1328 was divided into three lithostratigraphic units.

Lithostratigraphic Unit I (0–56.50 mbsf in Hole U1328B, 56.50–132.60 mbsf in Hole U1328C, 0–15.00 mbsf in Hole U1328D, and 0–92.26 mbsf in Hole U1328E) is characterized by fine-grained detrital sediments (dark greenish gray clay and silty clay) with abundant coarse-grained layers up to 6 cm thick indicative of turbidite deposits. The boundary between lithostratigraphic Units I and II is marked by a sharp decrease of sand and silt layers and by the onset of diatom-bearing sediments.

Lithostratigraphic Unit II (132.60–197.10 mbsf in Hole U1328C and 197.00–198.00 mbsf in Hole U1328E) is characterized by fine-grained (clay to silty clay) detrital sediments with some silty interlayers from turbiditic deposits and siliceous fossils. Abundant marine diatoms along with resting spores within lithostratigraphic Unit II suggests the diatoms bloomed in a shallow-water shelf environment associated with coastal upwelling, and then the diatoms were reworked. The boundary between lithostratigraphic Units II and III is distinguished by the sudden absence of diatoms.

Lithostratigraphic Unit III (197.10–300.00 mbsf in Hole U1328C) is characterized by fine-grained (clay to silty clay) detrital sediments with very few silty interlayers from turbidite deposits, likely deposited in an abyssal plain environment. The presence of authigenic carbonate cements show that diagenetic processes are active in lithostratigraphic Unit III. Because of the large input of turbidite deposits, in lithostratigraphic Unit I we see a significant increase in sedimentation rate from 24.6 cm/k.y. in lithostratigraphic Unit II to 37.5 cm/k.y. in lithostratigraphic Unit I.

At Site U1328, gas hydrate was sampled and evidence of gas hydrate was found in the recovered cores in the form of soupy and mousselike textures. At this site, soupy texture is only present within lithostratigraphic Unit I. At Site U1328 mousselike textures are present occasionally within lithostratigraphic Units I to III.

The LWD/MWD and wireline logged section in Holes U1328A and U1328C was divided into three "logging units" based on obvious changes in the downhole measured gamma ray, density, electrical resistivity, and acoustic measurements; for the most part these logging units correspond closely to lithostratigraphic Units I, II, and III.

Logging Unit 1 (0–128 mbsf in Hole U1328A) is characterized by a well-defined increase in density with depth. The most striking feature in this unit is seen in the LWD/MWD logs between the seafloor and 46 mbsf, where high resistivities (>25 m) alternate with intervals of much lower resistivity (1–2 m). The high resistivities likely indicate the presence of gas hydrate, which were sampled during coring.

Logging Unit 2 (128–200 mbsf in Hole U1328A) is marked at the top by a clear decrease in density log values. Unit 2 is also characterized by a constant relatively low background resistivity value just above 1 m and only one significant high-resistivity log-inferred gas hydrate occurrence at a depth of 160 mbsf.

Logging Unit 3 (200–300 mbsf in Hole U1328A) is characterized by small increases in background resistivity and notably more variability resistivity and P-wave velocity log values.

Physical properties were measured in cores recovered from four of the holes at this site, with the core-derived MAD data comparing favorably to both the LWD/MWD and downhole wireline data. Numerous low-porosity outliers, however, were interpreted to represent sand-rich samples.

It has been shown that RAB images as derived from the LWD/MWD GeoVision tool can be used to image gas hydrate in sediment. High concentrations of gas hydrate are evident in the interval 0–46 mbsf of Hole U1328A, where resistivities are high. The RAB images from Hole U1328A also reveal numerous high-resistivity sinusoidal features in the upper 46 mbsf in Hole U1328A and again at 90–100 mbsf, which can be interpreted as dipping fractures containing gas hydrate or possibly free gas. These near-vertical fractures may act as gas migration conduits that feed the gas hydrate accumulation observed near the seafloor.

To estimate the amount of gas hydrate at Site U1328, the GeoVision-derived resistivity logs were used as input to the Archie relation to estimate pore volume water saturations. Gas hydrate saturation is the percentage of pore space in sediment occupied by gas hydrate, which is the complement of the water saturation. These calculations have shown highly variable gas hydrate saturations in the upper 46 mbsf, with values as high as 95% in several intervals up to 10 m thick. These layers of high gas hydrate concentrations alternate with layers of much higher water saturations.

The combined analysis of acoustic velocities and waveform amplitudes can also help identify the occurrence of gas hydrate and/or free gas. In the interval between 210 and 220 mbsf, near the seismically inferred depth of the BSR at ~219 mbsf, the P-wave velocity drops slightly while the S-wave velocity increases. This could be due to the coexistence of free gas and gas hydrate in the vicinity of the BSR, which has been observed on Blake Ridge and Hydrate Ridge. Additional evidence for the occurrence of free gas below the BSR was noted in the analysis of the LWD/MWD acoustic coherence data, borehole fluid pressure response during drilling, and the wireline P-wave, resistivity, density, and neutron logs. The PCS degassing experiments of a single core in Hole U1328E also suggest the presence of a free gas phase below the BSR at this site (see below). However, it is important to note that the VSP survey obtained in Hole U1328C yielded a very uniform velocity profile with depth and no clear velocity contrast around the expected depth of the BSR.

Although we deployed the APCT, APC3, DVTP, and DVTPP temperature tools a total of nine times, we recorded only three reliable data points, which was mostly the result of severe ship heave conditions. The in situ temperatures determined for Site U1328 are generally similar to those at Site U1327 and slightly higher than those determined at similar depths during Leg 146. For Site U1328 we observed a seafloor temperature of ~3.5°C and a geothermal gradient of ~5.4°C/100 m, which corresponds to a predicted depth to the base of the methane hydrate stability zone ranging from 222 to 247 mbsf given the uncertainty in the data.

All cores from this site were systematically scanned upon arrival on the catwalk to detect IR anomalies indicative of gas hydrate dissociation during core recovery. Strong cold anomalies were detected in the shallowest cores from this site. A large amount of gas hydrate had been anticipated in the upper 30 mbsf based on LWD/MWD resistivity measurements and previous piston coring at this site (Riedel et al., 2002, in press; Solem et al., 2002), and a considerable amount was found. However, the LWD/MWD high resistivity–inferred gas hydrate occurrence at 90–100 mbsf in Hole U1328A was not seen on either the IR images or the wireline logs, both taken in Hole U1328C. The IR data may have missed this interval due to poor core recovery, but the lack of a high-resistivity layer in the wireline log points to horizontal inhomogeneity. This is not unexpected, in that the high-resistivity layer in the LWD/MWD image contains a steeply dipping fracture that is unlikely to be intersected at the same depth even in two closely spaced holes. The strongest anomalies were detected just above the seismically inferred BSR (210–222 mbsf), and a few small but distinct cold anomalies were observed below it, one of which exhibited pore water freshening indicative of the presence of gas hydrate (Core 311-U1328C-22X; ~249 mbsf). The possibility of gas hydrate beneath the BSR may indicate the presence of Structure II gas hydrate, which is stable below the base of the pure methane Structure I gas hydrate stability zone. However, it should be noted that there remains substantial uncertainty in the exact depth of the base of the gas hydrate stability field at this site and the depth of the BSR. All available data suggest that the gas hydrate stability zone could be deeper than the initially inferred depth of the BSR, which may result in shifting the observed IR anomalies to depths well within the gas hydrate stability field.

At Site U1328 we attempted 11 deployments of the 3 different pressure coring tools. The PCS was deployed six times at Site U1328 (twice in Hole U1328B, once in Hole U1328C, and three times in Hole U1328E), five of which recovered sediment under pressure. In addition to the PCS deployment, the HRC was used two times and the FPC was used three times, but none of these cores were recovered under pressure. Degassing of the five successful PCS cores from this site showed variable gas concentrations with depth. Two PCS cores were taken within the near-surface gas hydrate–bearing section from 0 to 46 mbsf (Core 311-U1328B-4P at 15 mbsf and Core 7P at 26.5 mbsf), which yielded 21.5 and 2.5 L of methane, respectively, equivalent to pore volume gas hydrate saturations of ~15% and ~2%. X-ray images of Core 311-U1328B-4P under pressure show 2–6 mm thick low-density structures that disappeared after degassing and are interpreted as gas hydrate veins. This core showed large amounts of gas expansion and sediment extrusion during depressurization, as did Cores 311-U1328B-7P and 311-U1328E-10P to a lesser extent. The two PCS cores taken in the Holes U1328C and U1328E at 92.0 mbsf (Cores 311-U1328C-5P and 311-U1328E-10P) each yielded quite different amounts of methane gas and would equate to the occurrence of 22% (Core 311-U1328C-10P) and 0.7% of gas hydrate (Core 311-U1328E-5P). One PCS core (Core 311-U1328E-13P) was taken from a depth of 233.0 mbsf, very close to the seismically inferred BSR depth. This core yielded 60 L of methane, the largest recovery of gas during this expedition. This amount of methane would fill 58% of the pore space if it was present as free gas or 50% if it was present as gas hydrate. However, gamma ray density scans during degassing and X-ray scans after depressurization showed almost no evidence of gas expansion cracks or large voids in the core. It is speculated that most of the gas released during degassing of this core came from the space between the inner and outer core barrel, where a gas bubble was observed during X-raying. Volumetric analysis suggests the presence of a 540 mL headspace in the outer core barrel which corresponds will to the 410 mL volume that would have been occupied by the released amount of gas at in situ conditions. The apparent extra gas in the PCS might have swabbed into the core barrel during the coring process.

A total of 91 interstitial water geochemistry samples were processed from four of the holes cored at Site U1328. The composite chlorinity profile for this site shows four distinct zones. In the upper ~30 mbsf, we see a striking increase in chlorinity, with maximum values exceeding 850 mM. The observed excess solutes are interpreted to result from salt exclusion from the water lattice structure during in situ gas hydrate formation that has not been removed by advective or diffusive processes. The second zone from ~30 to ~150 mbsf is characterized by relatively constant chlorinity values ranging from 538 to 570 to mM. A third zone, extending from ~150 to 250 mbsf, across the BSR, shows discrete excursions to fresher chlorinity values (as low as 348 mM), suggesting that gas hydrate was present in the cores and dissociated prior to processing the samples. The chlorinity anomalies are consistent with observations of distinct negative thermal excursions in IR scans. Our observations further indicate that most of the gas hydrates occupy relatively thin sand layers. In the deepest zone, below 250 mbsf, the chlorinity remains nearly constant at 493 tion with a fluid at greater depth that is notably different in composition from the deep-seated fluid sampled at Sites U1327 and 889/890.

To form and maintain shallow gas hydrate deposits near the seafloor, methane has to be supplied continuously. Furthermore, the shallow elevated chlorinity values would dissipate rapidly if they were not continuously maintained by ongoing gas hydrate formation. However, the chlorinity profile with depth at Site U1328 indicates a diffusion-controlled system. These observations indicate that the methane needed to sustain the shallow gas hydrate formation is likely supplied along faults or fracture zones, probably the ones imaged by the RAB tool within the gas hydrate–bearing section immediately below the seafloor.

The shipboard organic geochemistry program for Site U1328 included analysis of hydrocarbons and nonhydrocarbon gases from headspace gas samples, void gas samples, gas samples recovered during PCS degassing experiments, and gases from gas hydrate samples. Methane was the most prominent hydrocarbon gas in all of the samples analyzed; however, ethane was also present in almost all of the headspace samples. Most of the gas hydrate samples and gas hydrate–bearing sediments collected within the upper 46 mbsf under the vent site exhibited elevated ethane concentrations. These near-surface samples also contained slightly more air contamination and elevated H₂S concentrations. It is also notable that the concentration of ethane and other gas hydrate–forming gases, including propane and isobutane, increase within the gas samples collected from the cores crossing the depth of the seismically inferred BSR where the chlorinity and IR temperature anomalies both indicate evidence for gas hydrate. The occurrence of propane and elevated isobutane to n-butane (i-C₄/n-C₄) ratio support the hypothesis that the gas hydrates near the depth of the BSR may contain a mixture of Structure I and Structure II gas hydrates. It is also interesting that the ethane concentrations remain elevated below the depth of the BSR. Structure II gas hydrate is stable to greater depths with increasing temperature than Structure I gas hydrate; however, the observed IR and chlorinity anomalies are not necessarily below the base of the Structure I methane hydrate stability field and therefore not automatically related to Structure II gas hydrate given the uncertainty in the temperature measurements. However, the gas geochemistry does strongly suggest the presence of some mixture of Structure I and Structure II gas hydrates near the depth of the seismically inferred BSR.

Microbiological subsampling was routinely conducted on cores recovered from Holes U1328B and U1328C. On each core run PFT was continuously metered into the drilling fluid, and fluorescent microspheres were deployed on all cores in the continuously cored holes to investigate potential drilling fluid contamination of the core. These analyses confirmed that the center of each whole-round sample remains undisturbed for microbiological subsampling. Additional IR images were taken on the cut ends of each microbiological core section to document the thermal warming process of the core before subsampling.

The main objectives at this site were to

Apparently, however, only the very shallowest (<40 mbsf) and deepest (250–300 mbsf) portion of the sedimentary section cored at Site U1328 is dominated by fluid advection. It appears that diffusion transport controls the chemical depth profiles from ~40 to 250 mbsf at this site. This apparent contradiction can be explained with the vent model brought forward by Riedel et al. (in press). The model, based on various geophysical and geochemical observations, predicted that the shallow gas hydrate accumulations to be the result of isolated feeder channels or fractures. Along these fractures the bulk of the methane gas is transported upward and results in the near-seafloor concentrated gas hydrate accumulation. Evidence of the existence of these fractures comes from the LWD/MWD downhole logging data showing at several depths steeply dipping resistivity anomalies typical of fractures filled with gas hydrate or possibly free gas. These potential gas migration conduits may be connected to the seafloor chemosynthetic cold vent communities observed by bottom video surveys (Riedel et al., 2002, in press).

The growth of gas hydrate near the seafloor has also resulted in solute exclusion and development of high pore water salinities. This brine cannot be maintained in situ over a long period of time, unless gas hydrate is constantly formed at relatively high rates, thus showing the cold vent must be supplied with fluids and gas from greater depths. This is also indicated by the detection of a methane plume in the water column just above an active vent outlet. However, venting is most likely episodic since the methane plume is not always detectable. There is further evidence for the presence of Structure II gas hydrate at this site as seen by the presence of unusual amounts of propane and isobutane, which is unique when compared to the other sites cored during this expedition.

Various geophysical and geochemical data support the presence of a BSR at this site, as proposed by Riedel et al. (in press); however, the BSR at this site is difficult to identify with the available seismic data. The lack of good 3-D seismic velocity control could potentially result in misinterpretation of the existing two-dimensional (2-D) seismic data, in that the observed BSR may actually be a side diffraction and may not be exactly located beneath the active part of the cold vent and seismic blanking. In the LWD/MWD data a sharp decrease in electrical resistivity was observed at ~220 mbsf, although it is coincident with a high-density interval potentially related to the presence of carbonates. Acoustic wireline logging, however, shows a sharp discontinuity in P-wave and S-wave velocity at a depth of ~215 mbsf, close to the seismically inferred BSR depth of 219 this site yielded a temperature gradient of ~54°C/km, which predicts the base of gas hydrate stability at ~230 tries.

There is evidence for the occurrence of free gas at depths below the seismically inferred BSR, as demonstrated from pressure coring, LWD/MWD pressure monitoring, and elevated LWD/MWD electrical resistivity values. There are also seismic indicators for the occurrence of free gas below the BSR in the form of strong-amplitude anomalies. However, the VSP does not show any evidence of a velocity change over the entire logged interval from 105 to 285 mbsf, which will be further examined after the cruise.

Site U1329 (prospectus Site CAS-05D) is at the eastern end of the southwest-northeast–trending margin-perpendicular transect of sites occupied during this expedition and is located closest to shore (65 km) at a water depth of ~946 mbsl. The location of this site is interpreted to be at the eastern limit of gas hydrate occurrence on the Northern Cascadia margin.

The objectives of coring and downhole logging at this site are tied to completing the transect of scientific drill sites across the northern Cascadia margin to further constrain models for the formation of marine gas hydrate in a subduction zone accretionary prism. The depth to the BSR rapidly becomes shallower around this site and is only half the depth (~125 mbsf) than at Site U1327 (~225 mbsf) (Figs. F20, F21). At this eastern end-member site of gas hydrate evolution in the accretionary prism, the objectives include

Five holes were occupied at Site U1329 (prospectus Site CAS-05D) (Table T1). Hole U1329A was dedicated to LWD/MWD measurements to a TD of 220 mbsf. Hole U1329B consisted of only one missed mudline APC core to 9.5 mbsf. Hole U1329C was continuously cored (17 APC, 5 XCB, and 3 PCS cores; recovery = 99.3%) to 189.5 mbsf, and was terminated before the TD of 220 mbsf when the PCS cutting shoe broke off and was left in the bottom of the hole. The PCS was deployed three times in Hole U1329C, and four APC temperature measurements were made (APCT and APC3). Swell from a passing low-pressure system resulted in ship heave that was too high for wireline logging or coring operations, and we waited 4 h for the weather to improve. With a forecast for improving weather the following day, we decided to abandon Hole U1329C to drill a dedicated logging hole. Hole U1329D was drilled from the seafloor to 201.0 mbsf, which included another 1.5 h of suspended operations due to excessive ship heave, and a single XCB core was taken to 210.5 mbsf. Hole U1329D was wireline logged with the triple combo and FMS-sonic tool strings. The triple combo and the first pass of the FMS-sonic were logged to 209 mbsf. The second pass of the FMS-sonic only reached 171 mbsf. Hole U1329E was a special tool hole to 127.1 mbsf, where five APC cores were taken for high-resolution microbiological and geochemical studies, with two additional APC temperature measurements. Three DVTP deployments were also conducted. Five pressure cores were taken (three PCS, one HRC, and one FPC) separated by drilled intervals. In Figures F22 and F23, data from LWD/MWD logging (RAB images, porosity and Archie-derived pore water saturations), core-derived physical property data (porosity), and interstitial water chlorinity, as well as C₁/C₂ ratios from void gas samples are shown in comparison to the two key crossing seismic lines from this site.

Site U1329 is located near the foot of a relatively steep slope, and sedimentation at this site is dominated by slope processes. The stratigraphy at Site U1329 was divided into three lithostratigraphic units.

Lithostratigraphic Unit I (0–37.18 mbsf in Hole U1329C and 0–33.31 mbsf in Hole U1329E) is characterized by fine-grained detrital sediments (clay and silty clay), locally interbedded with coarse-grained sediments. Authigenic carbonates are abundant in some cores from Unit I, including the location of dolomite in Holes U1329C and U1329E, which coincides with changes in pore water Ca and Mg profiles, suggesting dolomite formation is an ongoing process. The sedimentation rate in Unit I appears to be relatively slow at ~10–12 cm/k.y. The boundary between lithostratigraphic Units I and II is defined by the first occurrence of diatom ooze.

Lithostratigraphic Unit II (37.18–135.60 mbsf in Hole U1329C and 33.31–125.95 mbsf in Hole U1329E) is characterized by a high abundance of biogenic silica (mainly diatoms). The sedimentation rate within Unit II appears to increase relative to Unit III from ~4 to 10 cm/k.y. The boundary between lithostratigraphic Units II and III is marked by a conglomerate composed of partly lithified and lithified rounded clasts supported by a silty clay matrix. The conglomerate at the base of Unit II corresponds to an unconformity between upper Miocene and Pleistocene sediments (no sediments preserved from 2–6.7 Ma) that also can be traced seismically for several kilometers along Line 89-08 (Fig. F20). The unconformity is not clearly seen in the higher-frequency seismic data crossing Line SCS CAS05C-01-04 (Fig. F21).

Lithostratigraphic Unit III (135 mbsf–TD) is characterized by fine-grained (clay to silty clay) detrital sediments with only a few coarser interlayers from turbiditic deposits. The input of detrital sediments from turbidites, however, is more obvious deeper in the section with the presence of nonmarine diatoms. In the lowermost part of Unit III, a breccia deposit marks a major change in deposition, possibly representing a debris flow. The sediments in lithostratigraphic Unit III were deposited at a low sedimentation rate of ~0.8–2.8 cm/k.y.

The biostratigraphy at this site was established by the analysis of diatoms. These analyses showed an interval of Quaternary sediments from the surface to ~35 mbsf that corresponds to lithostratigraphic Unit I. The age of lithostratigraphic Unit II was shown to range from 0.3 to 2.0 Ma. This interval showed an abundance of diatoms and resting spores suggesting a depositional environment typical of a coastal shelf area with upwelling. The sediments of this interval may also have been transported to this site from the shelf by turbidites. Sediments deeper than 137 mbsf, near the contact between lithostratigraphic Units II and III, contain diatoms of only late Miocene age (>6.7 Ma); thus, the Pliocene at this site is completely absent, representing ~4 m.y. of missing sediment, which was likely eroded.

The downhole logged section at Site U1329 was divided into three "logging units" based on obvious changes in the LWD/MWD and wireline gamma ray, density, electrical resistivity, and acoustic transit-time measurements.

Logging Unit 1 (0–130 mbsf), which corresponds to lithostratigraphic Units I and II, is characterized by low electrical resistivities and densities.

Logging Unit 2 (130–183 mbsf) is characterized by a small increase in resistivity and density compared to logging Unit 1. The top of logging Unit 2 corresponds to the bottom of lithostratigraphic Unit II, which was identified as an unconformity separating Pleistocene from upper Miocene sediments.

Logging Unit 3 (183 mbsf–TD) is characterized by an abrupt increase in electrical resistivity, density, and P-wave velocity, indicating an increasingly consolidated formation with lower log-derived porosities. Logging Units 2 and 3 correspond to lithostratigraphic Unit III.

Variations in physical properties do not correlate well with the lithostratigraphic and logging units. MAD analyses of porosity and bulk density as well as gamma ray attenuation density data from the multisensor track show anomalously uniform trends throughout most of the section cored from 25 to 180 mbsf. A slightly different trend is observed in the upper 25 mbsf where porosity rapidly decreases to values as low as 55%, coincident with the depth where rapid changes in the core-derived shear strength and electrical resistivity occur. Except for the top 15 mbsf, the magnetic susceptibility record shows extremely low and uniform values of <50 x 10^–7 SI. Grain densities generally decrease downhole crossing all lithostratigraphic boundaries starting from values of ~2.8 g/cm³ near the seafloor to ~2.6 g/cm³ at 175 mbsf, but this trend reverses below this depth and again reaches values as high as ~2.8 g/cm³. This deep increase in grain density and associated increase in bulk density occurs near the top of logging Unit 3, which is characterized by a sudden increase in electrical resistivity and drop in porosity. Analysis of the LWD/MWD density logs from this site yielded sediment porosities ranging from ~65% near the seafloor to ~23% at 220 mbsf.

IR imaging of the recovered core assisted in immediate gas hydrate detection on the catwalk. At this site, core IR temperatures did not show any significant cold spot anomalies from gas hydrate dissociation that could be related to the presence of gas hydrate in the recovered core. In situ temperature measurements with the APC3, APCT, and DVTP tools indicated a temperature gradient of 72° loor intercept of 3.34° –84 mW/m² for measured thermal conductivities of 1.0–1.1 W/m·K. This is consistent with the regional heat flow across the northern Cascadia margin (predicted to be ~72 mW/m² here) but higher than the heat flow measured at Site 889 during Leg 146, indicating that heat flow at this site in not affected by sedimentation and fluid expulsion.

In total six PCS deployments were made, three in Hole U1329C and three in Hole U1329E. Of the six deployments, two runs did not recover sediment under pressure and all other runs retrieved sediments under pressure. All PCS cores that were successfully retrieved under pressure were investigated by shipboard degassing experiments. In addition to the PCS, one HRC and one FPC were deployed in Hole U1329E. A full core at near in situ pressure was recovered by the HRC that revealed 10 cm high-velocity zones indicative of gas hydrate. The FPC deployment recovered a core without pressure. Degassing of the four PCS cores from this site that were recovered under pressure showed variable gas concentrations with depth. PCS Core 311-U1329C-7P (56.1 mbsf) and Core 311-U1329E-7P (74.0 mbsf) from within the predicted depth of the methane hydrate stability zone had total pore space methane concentrations of 79 and 85 mM, respectively, which would equate to a gas hydrate pore volume concentrations of <1% for both core samples. PCS Core 311-U1329E-10P (125.5 mbsf), from near the base of the predicted methane hydrate stability zone for this site, had a methane concentration of 89 mM, which falls below methane saturation at this depth, with no gas hydrate or free gas. The deepest PCS core (Core 311-U1329C-23P; 188.5 mbsf) was taken at a considerable depth below the base of the gas hydrate stability zone. This deep PCS had a total pore space methane concentration of 152 mM, which suggests a potential pore volume free gas saturation of 2.4%. A potential gas release during the coring operation may cause this to be an overestimate, yet it still supports the presence of free gas below the BSR at this site.

Interstitial water analyses were carried out on samples from Hole U1329C with additional high-resolution sampling in the top 15 mbsf of Hole U1329E to capture the SMI. Interstitial water salinities decrease from ~34 to ~30 at a depth of ~50 mbsf but remain almost constant at values of ~30.5 until near the bottom of the cored section in Hole U1329D. The deepest water samples from this site (>180 mbsf) show a sharp drop in salinities, ranging from 22 to 28. A distinct chlorinity minimum (~15 mM decrease relative to the rest of the trend) is observed at the projected depth of the seismically inferred BSR. Assuming that this chlorinity minimum is the result of gas hydrate dissociation during core recovery and handling, the observed chlorinity minimum would equate to ~2% in situ pore space filling of gas hydrate. The strong decrease in chlorinity and salinity below 180 mbsf are coincident with the pronounced increase in electrical resistivity in the LWD/MWD downhole logging data in logging Unit 3 and suggests communication with a deeper-sourced fresher fluid. The Ca and Mg depth profiles reflect carbonate and dolomite formation in the shallow section (SMI–60 mbsf) but also suggest commingling with a deeper-sourced fluid over a depth range from 60 mbsf to the BSR.

Organic geochemical studies at Site U1329 included analysis of the composition of volatile hydrocarbons (C₁–C₅) and nonhydrocarbon (i.e., O₂ and N₂) gases from headspace gas samples, void gas samples, and gas samples recovered during PCS degassing experiments. The predominant hydrocarbon gas found in the cores from Site U1329 was methane; however, we did see an increase in ethane concentrations in the void gases collected from the stratigraphic section overlying the projected depth of the BSR. This increase in ethane concentrations near the BSR can also be seen in the plot of the C₁/C₂ void gas ratios. Other studies have shown void gas ratios (such as C₁/C₂) can be elevated in a gas hydrate with the preferential selection of ethane into the gas hydrate structure. But the observed increase in the C₁/C₂ ratio below the projected depth of the BSR may be more indicative of a methane-enriched free gas accumulation. The C₁/C₂ ratios were generally high, suggesting a microbial origin for the observed methane. The samples collected from deeper than 180 mbsf at this site also exhibited significant increases in C₂–C₅ concentrations, which suggests the influence of a potential thermogenic hydrocarbon source.

Microbiological subsampling was routinely carried out on cores recovered from Hole U1329C. On each core run PFT was continuously metered into the drilling fluid, and additional fluorescent microspheres were deployed on selected cores to investigate potential drilling fluid contamination of the core. These analyses confirmed that the center of each whole-round sample remains undisturbed for microbiological subsampling. Additional IR images were taken on the cut ends of each microbiological core section to document the thermal warming process of the core before subsampling.

When considering the primary research objectives of this site, one of the most important features is its location on the relatively steep slope and the observation that sedimentation at this site is dominated by both slope turbidite deposition and erosional processes. The presence of thick turbidite sequences, including the presence of nonmarine diatoms in the stratigraphic section, is a testament to the history of slope-dominated processes. The occurrence of a significant depositional hiatus or erosional event that juxtaposes Miocene with Pleistocene sediments at this site further documents the complex depositional history of this margin. The deepest core and downhole logging penetrations at this site also revealed even a more complex geologic history with unique high-resistivity, low-porosity conglomerate deposits that may represent thick debris flows.

Geochemical analyses of recovered gas samples and interstitial fluids have also documented a relatively complex fluid regime for this site. The relatively low interstitial fluid chlorinities observed near the seafloor may reflect paleoceanographic changes in seawater salinity. However, the more rapid Cl concentration decrease with depth strongly suggests communication with a deep-seated, fresher fluid, especially below 140 mbsf. For the most part, geochemical analyses of gases from this site reveal a similar story as the analysis of interstitial fluids, with most of the cored section dominated by a simple methane gas-rich system. But near the bottom of the cored section there are indications for the influence of a deeper hydrocarbon source.

Identifying gas hydrate and supportive physical evidence of the BSR at this site remains an elusive goal. As seen in Figures F20 and F21, the BSR is subtle at this site and is located only ~10 m above a prominent unconformity, which results in a complicated reflectivity pattern. The precoring LWD/MWD and conventional wireline logging data were used to identify and further characterize potential gas hydrate and related free gas occurrences at each site occupied during this expedition. The presence of gas hydrate is generally characterized by increases in measured electrical resistivities and acoustic velocities. The relative lack of notable resistivity or acoustic downhole log anomalies at this site supports a general inference of very low to no gas hydrate occurrence at this site. The lack of either visual observations of gas hydrate or the occurrence of IR-detected thermal anomalies along the recovered cores also supports the assumption that this site contains little to no gas hydrates. However, geochemical analyses of interstitial fluids from near the depth of the predicted BSR may suggest the presence of a small amount of gas hydrate, with minimum dissolved chloride concentration at ~125 mbsf, coincident with the depth of the BSR. The HRC core taken from 114.6 mbsf, which contained high-velocity layers, also suggests the presence of gas hydrate at these depths. In addition, the relative increase in ethane concentrations immediately above the depth of the BSR may indicate the presence of gas hydrate. Degassing experiments of three PCS cores that were collected from within the zone of predicted methane hydrate stability appear to confirm that this site contains very little gas hydrate, if any. However, a PCS core from 188.5 mbsf in Hole U1329C does suggest the occurrence of a free gas phase. The presence of free gas at greater depth below ~160 mbsf may also be supported by a distinct change in seismic reflection character in the low-frequency seismic data of Line 89-08 (Figs. F21, F23). In contrast to the shallower section of the seismic line above 1.5 s two-way traveltime (TWT), no clear reflection can be identified below and seismic frequency also is strongly reduced.

As noted, this site was intended to characterize the eastern limit of gas hydrate occurrence on the northern Cascadia margin and establish an understanding of the geologic controls on the occurrence of gas hydrates along the transect of sites established during this expedition. All of the objectives set for Site U1329 are considered fulfilled.