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doi:10.2204/iodp.proc.340.101.2013

Principal results

Site U1393

Background and objectives

IODP Site U1393 (proposed Site CARI-02C; 16°43.13′N, 62°5.06′W; 914 meters below sea level [mbsl]) is located close to the Soufrière Hills Volcano on Montserrat (7.4 nmi [13.7 km] from Point Shoe Rock, at the southeast tip of Montserrat) (Fig. F2; Table T1).

The ongoing eruption of the Soufrière Hills Volcano on Montserrat started in 1995. Activity has included lava dome growth, pyroclastic flows from dome collapse, explosive activity with tephra fall and pumice flows, flank collapse with debris avalanches, and volcanic blasts. More than 70% of erupted material from the ongoing eruption has been transported to the sea (Le Friant et al., 2009, 2010; Trofimovs et al., 2006). The rapid deposition of volcanic material into the sea has caused small tsunamis (Herd et al., 2005).

Site survey data indicated that distal parts of the pyroclastic flows and some underlying, older chaotic deposits interpreted as debris avalanches have been deposited at Site U1393. The English’s Crater event, which occurred ~2000 y ago, produced Deposit 1 (Boudon et al., 2007). The deeper deposit (Deposit 2) probably resulted from a combined submarine and subaerial mass-wasting process of the eastern flank of the volcano, which included failure and deformation of submarine sediment (Le Friant, 2004; Lebas et al., 2011; Watt et al., 2012). Seismic data indicated that drilling at Site U1393 could penetrate through the erupted material from the ongoing eruption and into the underlying Deposits 1 and 2.

The objective for Site U1393 was to characterize the processes occurring during debris avalanche emplacement, associated erosional processes, and tephra diagenesis. Analysis of 5 m piston cores taken in this area shows that pyroclastic material from the 2003 Soufrière Hills Volcano lava dome collapse mixed with seawater and immediately deposited the coarse components out of suspension (Trofimovs et al., 2006). Study of the coarse debris avalanche deposit will enhance our understanding of emplacement processes.

Comparing the geochemical signatures (pore water and sediment) of cored material with surface sediment (from the 2007 NERC cruise) will allow us to characterize the alteration rates of volcanic material in seawater. In addition, we will examine the dependency of alteration rate and style on grain size, layer thickness, and admixture of sediment.

Cores from Deposit 1 (smaller volume) and Deposit 2 (larger volume) will allow us to compare the emplacement processes of mass-transport deposits of different magnitudes. We plan to undertake a detailed lithologic, sedimentologic, and textural fabric analysis of the retrieved material at macro- and microscopic scales to investigate transport and deposition processes, the nature and magnitude of erosional processes, and interaction with the substratum (e.g., bulking) (Komorowski et al., 1991; Glicken, 1991, 1996). These data will provide valuable insights into chronology (one or several pulses) and debris avalanche mobility, which have implications for tsunami genesis.

Scientific results

Lithostratigraphy

Based on the lithologic characteristics of sediment recovered at Site U1393, only one lithostratigraphic unit, Unit A, was defined (Fig. F5). Unit A extends from the seafloor to 4.24 mbsf; however, the lower stratigraphic boundary of this unit cannot be defined because of poor core recovery. The upper part of Unit A consists of mud clasts embedded in a sandy matrix. This lithology is followed downhole by dark brownish gray-black sand consisting of volcaniclastic material containing medium to very coarse sand-sized grains. Grains are composed mainly of andesite and rarely of carbonate. Occasionally, larger clasts of amphibole-rich andesite are present. The unit is moderately well to well sorted, massive, and normally graded. The lowest part of Unit A consists of andesite clasts as large as 3 cm embedded in a coarse sand matrix. Below Unit A, the material recovered consists mainly of andesite clasts. These clasts show variable signs of hydrothermal alteration and subaerial oxidation, and some large clasts were abraded and possibly broken during coring and recovery. The uppermost 4.24 m of the material cored is a product of the most recent eruption of the Soufrière Hills Volcano.

Paleontology and biostratigraphy

Generally, the core catchers retrieved at Site U1393 contain very few micro- and nannofossils, which is consistent with the lithostratigraphic information at this site. Because of the small number of fossils, an age determination of the cored material was not possible. However, the four observed benthic foraminifers are typical for a shallow-water reef environment, suggesting transport and reworking.

Physical properties

Physical properties data obtained on the cored material are typical of well-sorted sand with an andesitic bulk composition (Fig. F5). The measured grain density of 2.80 g/cm³ and the measured bulk porosity of 42% are consistent with an andesitic composition and medium- to well-sorted sand that has undergone little consolidation. Magnetic susceptibility (maximum value of 2550 × 10^–5 SI at 1.07 mbsf) of the material dominated by volcaniclastic particles is much higher than that in hemipelagic sediment. Mean P-wave velocity is 1750 m/s.

Paleomagnetism

Meaningful paleomagnetic directions for the interpretation of the geomagnetic field at Site U1393 could not be obtained, primarily because of the sediment composition, sediment grain size, and consolidation state of the material recovered.

Site U1394

Background and objectives

IODP Site U1394 (proposed Site CARI-03C; 16°38.43′N, 62°2.29′W; 1115 mbsl) is located off the island of Montserrat (~13 nmi [24 km] from Point Shoe Rock, at the southeast tip of Montserrat) (Fig. F2; Table T1).

Site survey data obtained for Site U1394 revealed the presence of chaotic deposits interpreted as debris avalanche deposits (Deposit 2 and underlying Deposit 8) and indicated that drilling could penetrate through multiple units of debris avalanche Deposit 2 (Lebas et al., 2011; Watt et al., 2012). We planned to drill 244 m through volcanic and biogenic sediment with intercalated chaotic debris avalanche Deposit 2.

The objective for Site U1394 was to characterize processes that occur during debris avalanche emplacement and associated erosional processes. Study of the sediment overlying the mass-transport deposit will allow us to date the associated event using δ¹⁸O chronostratigraphy. We will be able to determine whether the mass-wasting process occurred as a single event or as a series of closely spaced, separate events. Utilizing a combination of detailed lithologic, sedimentologic, and textural fabric analyses, we will be able to test the hypothesis that the debris avalanche incorporated sediment eroded from the seafloor during its emplacement. We hoped to reach the bedded units below the chaotic debris avalanche unit and thus investigate the textural and structural characteristics of the base of the debris avalanche (Komorowski et al., 1991; Glicken, 1991, 1996). Existing numerical models of debris avalanche emplacement do not sufficiently consider the interaction of the debris avalanche with the substratum and its influence on the mobility of the flow. Our goal was to look for structural evidence of the development of shear zones from the base of the debris avalanche into the overlying plug and fluidization structures (clastic dikes) described in terrestrial debris avalanche deposits (e.g., Glicken, 1996; Voight et al., 2002; Gee et al., 1999; Clavero et al., 2002; Shea et al., 2008).

Scientific results

Lithostratigraphy

The main lithologies cored at Site U1394 are hemipelagic mud, turbiditic sand and mud, mafic volcaniclastics, and tephra (Figs. F6, F7). The hemipelagic mud mainly consists of fine-grained calcareous biogenic fragments and siliciclastic sediment. It is often pale yellowish gray to dark gray in color, varies from fine silt to fine mud in grain size, and is moderately to poorly sorted. The turbiditic sand and mud lithology is characterized by normally graded, massive, well-sorted mud (for thin deposits a few centimeters thick) to very coarse sand (for meter-thick deposits) consisting of volcaniclastic and bioclastic particles. Volcaniclasts include fragments of fresh andesitic lava and pumice, altered lava, and crystals (feldspar, amphibole, etc.). Bioclasts include fragments of carbonate materials such as coral and shells. The ratio of volcaniclastic to bioclastic components varies. Mafic volcaniclastics consist of basaltic turbidites. Tephra deposits retrieved from this site are composed of fining-upward units of normally graded (from pebble to fine sand) basaltic particles and basaltic scoria. The fining-upward units vary in thickness from 6 to 13 cm (Hole U1394A) and from 13 to 30 cm (Hole U1394B).

Investigation of the main lithologies by X-ray diffraction (XRD) shows that the pelagic sediment intervals predominantly contain calcite and high-Mg calcite plus or minus aragonite, together with minor volcanic phases (mostly plagioclase with lesser orthopyroxene and hornblende) and amorphous clay minerals. Samples from the volcaniclastic horizons contain dominant plagioclase and lesser amounts of orthopyroxene and hornblende, as well as minor sedimentary carbonate. One of the investigated tephra layers contains abundant smectite in addition to the volcanic minerals and background pelagic phases noted above. The CaCO₃ content of the cored material is higher in the largely pelagic sections, with some values >60%, than in the units more dominated by volcanic turbidites. However, the presence of smaller quantities (i.e., <20%) of CaCO₃ in the latter still indicates a biogenic component and is consistent with visual inspection of the core. Organic carbon concentrations in the pelagic sections range as high as 1 wt% or higher, with values in the turbiditic section as low as <0.2 wt%.

Based on abrupt or gradational changes in the abundance of these lithologies and distinctive marker horizons (tephras and turbidites), six lithostratigraphic units, termed Units A–F, were defined. Unit A is divided into seven subunits (A-1 to A-7). Unit A (~7 m thick) consists of a series of volcaniclastic turbidites with varying proportions of bioclastic particles separated by variably thick hemipelagic sediment consisting of mud to rarely silty mud. Turbidites generally fine upward from a sandy base into a muddy top. A basaltic tephra layer marks the base of the unit. Unit B is ~43 m thick. The upper part of Unit B consists of a fairly thick interval of relatively coarse grained, stacked, and amalgamated turbidites ranging in composition from bioclastic to volcaniclastic. The turbidites are always massive and planar with ripple cross-lamination always absent, suggesting rapid deposition that prevented bed-load reworking into laminae. Below this interval, turbidites are flat lying, relatively thin, and sometimes weakly deformed. The thick turbidite interval is separated from the thin layer of turbidites by an interval of very contorted hemipelagic silty mud with fine laminae. Unit C (~24 m thick) contains alternating sequences of hemipelagic sediment and volcaniclastic turbidites. Individual intervals of hemipelagic sediment are as thick as 130 cm. Unit D (~18 m thick in Hole U1394A; 36 m thick in Hole U1394B) is dominated by massive coarse-grained turbiditic sand composed of variable amounts of volcaniclastic and bioclastic material. Turbidites are either graded or ungraded. Chaotically distributed clasts (andesitic and biogenic) up to several centimeters in length in some ungraded sections may suggest en masse emplacement by debris flows. Unit E (~90 m thick in Hole U1394A; ~70 m thick in Hole U1394B) contains significant amounts of hemipelagic mud alternating with turbidites, which consist mainly of volcaniclastic or bioclastic material or a mixture of both. The upper part of Unit E contains relatively thick and coarse-grained turbidites; turbidites are less abundant and thinner in the middle part of Unit E. Turbidite thickness increases again near the base of the unit. Distributed throughout Unit E are massive brown ash layers, some of which are 20 cm thick, and layers of pumice clasts (as wide as 5 cm in diameter). Unit F (~35 m) is only recognized in Hole 1394A and its base was not reached. It is poorly recovered, but consists of coarse-grained andesitic clasts.

A closer investigation of the volcaniclastic and fallout deposits based on thin section microscopy shows that recovered clasts of andesitic lava and pumice fragments consist of plagioclase (70%), amphibole (25%), Fe-Ti oxides (4%), and orthopyroxene phenocrysts (1%). In the andesites, phenocrysts are contained in a microcrystalline matrix of plagioclase, oxides, and pyroxene microlites. The groundmass of the investigated pumice particles is significantly different. It consists of glassy material exhibiting considerable flow lineation. No flow lineation was observed in the lava clasts. The groundmass to phenocryst ratios are approximately 60:40 and 70:30 for andesite and pumice, respectively. Microscopic investigation of the tephra layers revealed that the uppermost tephra layer is basaltic in composition, containing fragments of plagioclase, olivine, clinopyroxene, and oxides in descending abundance. The deeper layers are of basaltic andesitic or andesitic composition, containing fragments of plagioclase, amphibole, orthopyroxene, and Fe-Ti oxides.

Paleontology and biostratigraphy

The microfossil content of the sediment described above are consistent with their intensely reworked nature. Calcareous nannofossils and planktonic and benthic foraminifers of varying abundances and levels of preservation were observed. Volcanic clasts, coral fragments, highly fragmented foraminifers, and abundant reef-dwelling benthic foraminifers are observed in the majority of core catcher samples. Biostratigraphic datums derived from both calcareous nannofossils and planktonic foraminifers show that Site U1394 contains many levels of reworked sediment from the early Pleistocene amidst a background of late Pleistocene sedimentation.

The observed nannofossils generally show extremely poor preservation, and their abundance is low. Typical nannofossil species observed within the cored sediment are Gephyrocapsa caribbeanica, Pseudoemiliania lacunosa, Calcidiscus leptoporus, and Helicosphaera kamptneri. Helicosphaera inversa is a very important species because of its short range through the early and late Pleistocene (upper Zone CN13 through Zone CN14), assigning the cored materials to the Pleistocene. Reworking of the sediment is also indicated by the occurrence of Helicosphaera sellii (Zones CN10–CN13) in a number of samples. Globigerinoides ruber (white) and Globigerinoides sacculifer dominate the planktonic foraminifers observed at Site U1394. Other abundant species include Globigerina falconensis, Globigerinita glutinata, Globigerinoides elongatus, Globorotalia tumida, and Neogloboquadrina dutertrei (dextral). Planktonic foraminifer species present are indicative of warm subtropical waters. Three marker species were commonly encountered—Globorotalia flexuosa (0.07–0.40 Ma), Globigerinella calida (base occurrence [B] at 0.22 Ma), and Globorotalia tosaensis (top occurrence [T] at 0.61 Ma)—assigning the investigated sediment, in accordance with nannofossil observations, to within the Pleistocene. The presence of the benthic foraminiferal species Osangularia, Globocassidulina, Cibicides, and Laticarinina pauperata suggests a bathyal paleodepth for Site U1394.

Paleomagnetism

Through measurement of the natural remanent magnetization (NRM) all superconducting rock magnetometer (SRM) and discrete inclination data record normal polarity. We see no evidence for reversed polarity in the record, particularly in the lower part of the record where data coverage is better. Because of the lack of a continuous record, we cannot unequivocally say that all sediment was deposited within the Brunhes chron; however, this would indicate a late Pleistocene age for the site, which agrees with biostratigraphic ages.

Physical properties

Physical properties of material retrieved at Site U1394 can generally be correlated to lithologic variations, including composition, grain size, and observed lithification (Figs. F6, F7). Bioclastic and volcaniclastic turbidites, as well as thick tephra layers, can be discerned from background sedimentation (carbonate ooze) by most of the physical properties (Fig. F7). The hemipelagic mud generally shows little variation and has low magnetic susceptibility (200 × 10^–5 to 400 × 10^–5 SI), low P-wave velocity, and relatively high natural gamma radiation (NGR). In contrast, the physical properties of turbidites are relatively heterogeneous, with overall high values of magnetic susceptibility (average = 740 × 10^–5 SI) and P-wave velocity but low NGR. This is typical for these materials, as the products of volcanic eruptions usually have higher iron content than hemipelagic sediment, whereas NGR is usually higher in hemipelagic sediments (e.g., U content in hemipelagic sediment is higher than that found in volcanic products). Single bioclastic and volcaniclastic turbiditic units throughout both holes can be traced by their uphole monotonically decreasing values in magnetic susceptibility, P-wave velocity, and density, mimicking their grading in grain size. A sharp drop in each of these values occurs at the boundaries of the turbiditic units. Where sufficiently thick, ash layers give positive peaks in magnetic susceptibility. Between 10 and 15 mbsf, magnetic susceptibility, density, and NGR data systematically differ in Holes U1394A and U1394B. This pattern is consistent with differences in lithologies retrieved from both holes. Hole U1394A is dominated by dark, dense turbidites with andesitic composition at this interval, whereas lighter colored pumice-rich deposits were cored in Hole U1394B. P-wave velocity averaged 1614 m/s. The mean thermal conductivity is 1.03 ± 0.07 W/(m·K) with a standard error on the mean of 0.01 W/(m·K). These values are similar to expected values for high-porosity sediment. The measured porosity of hemipelagic samples ranges from 48% to 66%. Turbidites display porosity values between 42% and 60%. Bulk density of the hemipelagic sediment ranges from 1.52 to 1.85 g/cm³, whereas bulk density of the turbiditic sediment ranges from 1.65 to 2.08 g/cm³. Grain density values of the hemipelagic sediment exhibit a narrow range of 2.63–2.79 g/cm³, whereas grain density values obtained from turbidite samples show a slightly larger range of 2.6–2.9 g/cm³. Turbidites consisting of a mixture of bioclastic and volcaniclastic material have grain densities ≤2.79 g/cm³.

Downhole logging

In situ measurements of geophysical properties obtained by downhole logging operations are in general agreement with physical properties data obtained from the cores (Fig. F7). Gamma radiation data do not exhibit a clear downhole trend over the measured interval, but generally the fine-scale variations in total gamma radiation have a higher frequency above 110 mbsf than below this depth. This change seems to coincide with a change from stacked turbidites into a series of alternating turbidites and hemipelagic sediment. Sonic velocities generally increase downhole, ranging from ~1650 to 1900 m/s. Distinctive local peaks in compressional velocity (V_P) coincide with increased resistivity and magnetic susceptibility, corresponding most likely to similarly scaled turbiditic units identified in the cores.

Geochemistry

In addition to studies done on retrieved sediment, pore water samples obtained from hemipelagic sediment were also analyzed. Pore water samples from turbiditic units were generally not obtained because it is not possible to collect meaningful pore water data from such highly permeable material. Pore water samples were largely taken from intervals dominated by pelagic carbonate. Alkalinity values increase from 3.3 mM in the uppermost section to a consistent value of 11.5 mM at roughly the middle of the hole before decreasing to 7.5 mM at the base of the hole. pH values remain relatively constant at 7.4–7.5 throughout the hole. Of the major cations, calcium decreases from values close to bottom water in the uppermost sample to a minimum at roughly the middle of the hole before increasing toward the bottom, whereas magnesium monotonically decreases with depth, with the exception of the deepest sample (Fig. F7). Sodium and potassium concentrations show a weak increase and decrease with depth, respectively. ΣS concentrations show a similar pattern to those of calcium. Chloride concentrations fluctuate within the normal range (550–580 mM) expected for pore water obtained from squeezing carbonate sediment. Generally, pore water data are consistent with diagenesis of carbonate-rich sediment with organic carbon concentrations that are typical of an open marine setting.

Site U1395

Background and objectives

IODP Site U1395 (proposed Site CARI-04D; 16°29.60′N, 61°57.09′W; 1191 mbsl) is located between Guadeloupe and Montserrat (Fig. F2; Table T1).

According to the site survey data, Site U1395 is located beside Deposit 2. Seismic reflection profiles indicated that drilling at Site U1395 could penetrate a succession of hemipelagic sediment and turbidites. The proposed total depth for this site was 244 mbsf.

The objective for Site U1395 was to characterize the sedimentation processes related to volcanic activity in the Bouillante–Montserrat half graben. We planned to drill through hemipelagic sediment, turbidites, and tephra to retrieve a complete record of sediment. Work around the Canary Islands has shown that distal volcaniclastic turbidites generated by collapse events can be used to study the gross character of landslide emplacement (Wynn and Masson, 2003; Hunt et al., 2011). Results from ODP Hole 1223A off Hawaii identified the association of several turbiditic deposits with landslides, showing that the Koolau Volcano collapsed repeatedly and that landslides constituted a greater risk than previously thought (Garcia et al., 2006). Analysis of cores taken during the JCR123 cruise suggests that distal turbidites associated with Montserrat provide a record of all main pyroclastic flow events that entered the ocean during the current eruptive phase (since 1995). Information from these cores also records the waxing and waning phases of individual dome collapses (Trofimovs et al., 2006). Turbidites in cores recovered from this site should therefore provide a record of dome and flank collapses. With the retrieved material, it will also be possible to better constrain the long-term sedimentation rate in the northern part of the arc.

Scientific results

Lithostratigraphy

The main lithologies cored at Site U1395 resemble those cored at Site U1394 (Figs. F8, F9). Based on abrupt or gradational changes in the abundance of these lithologies or on distinct marker horizons (e.g., tephra layers), the material was divided into nine lithostratigraphic units (Units A–I). Generally, each unit consists of various combinations of hemipelagic mud, turbiditic sand and mud, and tephra. Unit A is ~10 m thick and is similar to Unit A at Site U1394. It consists of volcaniclastic and mixed bioclastic-volcaniclastic turbidites interbedded with hemipelagic background sediment. Unit A is divided into seven subunits (A-1 to A-7). Unit B is ~6 m (Hole U1395A) and 4 m (Hole U1395B) thick and consists of a sequence of thick, stacked volcaniclastic turbidites, showing normal grading from very coarse to very fine sand. The matrix of these turbidites is mainly composed of dense to vesicular lava fragments, pyroxenes, amphiboles, and feldspars with a very low, or no, carbonate fraction. Occasionally, larger pumice clasts (as large as 2 cm) are present in this unit. Unit C consists of a 65 cm thick layer of hemipelagic sediment. Unit D, which is ~2 m (Hole U1395A) and 3 m (Hole U1395B) thick, is composed of another sequence of thick, stacked volcaniclastic turbidites similar in appearance to the turbidites in Unit B. However, in Hole U1395B, Unit D turbidites show a much higher content of large pumice (1–4 cm in diameter) particles dispersed throughout the entire matrix of the turbidites. Unit D is followed by a thick sequence (43 m) of mainly hemipelagic sediment, defined as Unit E. Intercalated throughout this sequence are a small number of relatively thin sandy turbidites, consisting of volcaniclastic, bioclastic, or mixed bioclastic-volcaniclastic particles. Additionally, several volcanic fine sand layers are identified in this unit, as well as some partly well sorted pumice deposits. Unit F is ~19 m thick and is also composed of thick, stacked turbiditic sequences interrupted by hemipelagic sediment. Unit F is divided into three subunits (F-1 to F-3). The upper part of Unit F (Subunit F-1) is composed of a thick, dark, homogeneous turbidite consisting of mixed bioclastic-volcaniclastic material. The majority of this turbidite is ungraded, with normal grading occurring only in the uppermost part, followed by a layer of hemipelagic sediment with intercalated layers of sand-sized bioclastic and volcaniclastic particles. These layers are massive to normally graded, changing from very fine to medium sand. The lower part of Unit F (Subunit F-2) is mainly composed of hemipelagic sediment with intercalated sandy bioclastic or volcaniclastic layers. Unit G (~31 m thick) is divided into two subunits (G-1 and G-2). Subunit G1 consists of hemipelagic sediment interbedded with sand-sized volcanic material consisting of lava fragments, scoria, plagioclase, pyroxene, and rare amphibole. Amphibole appears only in a few layers (without clinopyroxene) and is characteristic of tephra deposits originating from volcanoes in the central part of Guadeloupe. Tephras are particularly abundant between 90 and 100 mbsf (Core 12H for Holes U1395A and U1395B). In Hole U1395B, a succession of volcaniclastic turbidites also occurs in Subunit G-1. Subunit G-2 is characterized by highly contorted and deformed hemipelagic sediment. Unit H, which is ~8–11 m thick, is composed of a thick sequence of pumice-rich turbiditic deposits showing normal grading, with a matrix dominantly composed of crystals, lava clasts, and minor pumice and carbonates. Unit I (121 mbsf to the base of Hole U1395A and 124 mbsf to the base of Hole U1395B) consists of semiconsolidated silt- and mudstones, most of which are heavily bioturbated.

XRD and carbonate analysis performed on 44 individual samples taken throughout the entire cored interval shows results similar to analyzed samples from Site U1394. Samples of pelagic sediment are characterized by calcite, high-Mg calcite plus or minus aragonite, and minor volcanic phases such as plagioclase, orthopyroxene, and hornblende. The clay minerals detected are kaolinite, smectite, and glauconite. Samples from the volcanic-rich horizons contain dominant plagioclase, lesser amounts of orthopyroxene and hornblende, and minor carbonate.

CaCO₃ content is much higher in the largely pelagic sections in the upper part of this hole (>30%) than in the largely volcanic turbidites. The presence of a few weight percent CaCO₃ in the latter indicates a significant biogenic component. CaCO₃ content is highest (as high as 88%) in the semilithified sediment toward the base of the hole. Organic carbon concentrations in the pelagic sections can exceed 1 wt% but are much lower in the turbidite sections. Organic carbon concentrations also increase toward the base of the hole (as high as 1.5 wt%). The ratio of organic carbon to CaCO₃, however, remains relatively constant in hemipelagic intervals throughout the hole, suggesting that the concentration increases simply reflect less dilution by volcanic material at depth.

Paleontology and biostratigraphy

Biostratigraphic studies of the cored material were limited by its coarse nature. Site U1395 core catcher samples contain calcareous nannofossils and planktonic and benthic foraminifers of varying abundances and at varying levels of preservation. Generally, preservation deteriorates with depth, making the samples increasingly difficult to date. Both nannofossil and planktonic foraminiferal biostratigraphic datums for this site indicate ages of deposition ranging from late Pleistocene to early Pleistocene. Three different nannofossil assemblages were observed with increasing depth: first, within the top this site are Geophyrocapsa oceanica, Rhabdosphaera clavigera, Geophyrocapsa muellerae, Helicosphaera kamptneri, and Helicosphaera hyalina. Pseudoemiliania lacunosa was not found in the uppermost core at this site, dating the uppermost sample to <0.289 Ma. Below, typical species present were P. lacunosa, Ceratolithus cristatus, H. hyalina, Calcidiscus leptoporus, R. clavigera, Calciosolenia murrayi, and Syracosphaera pulchra. Lastly, in the lower portion of the site, a nannofossil assemblage typical for the early Pleistocene with Gephyrocapsa caribbeanica, P. lacunosa, Coccolithus leptoporus, and Crenalithus doronicoides was observed. C. doronicoides was detected in Sample 340-U1395A-12H-CC, the first sample below the lowest occurrence of G. oceanica, indicating that this sediment is within nannofossil Subzone CN13b. The assemblage of planktonic foraminifers observed in the cored material is generally characteristic for subtropical waters and is dominated by Globigerinoides ruber (white) and Globigerinoides sacculifer. Other abundant species include Globigerina falconensis, Globigerinita glutinata, Globigerinoides elongatus, Globorotalia tumida, and Neogloboquadrina dutertrei (dextral). Three biozones were recorded, PT1b, PT1a, and PL6, with PL6 in the bottom sample of this site. The primary marker between Zones PT1a and PL6 was not recorded; however, Zone PL6 was recognized based on the presence of Globorotalia exilis (T 2.1 Ma) instead, a secondary datum within Zone PL6. Several additional secondary datums were recorded as well: Globorotalia flexuosa (0.07–0.40 Ma), Globigerinella calida (T 0.22 Ma), and Globorotalia tosaensis (T 0.61 Ma). The presence of the benthic foraminiferal species Uvigerina auberiana, Laticarinina pauperata, Bulimina aculeata and the genus Osangularia suggests a bathyal paleodepth for this site. In addition to the micro- and nannofossils obtained at this site, sponge spicules, pteropods, and heteropods are also abundant and generally well preserved in the upper samples. Otoliths are present throughout the core samples, and four different morphotypes are present. Ostracods when present are rare.

Paleomagnetism

Interpretation of the NRM of the recovered cores is based on the hemipelagic sediment, as it is potentially the least disturbed and most optimal sediment to hold information about the behavior of the geomagnetic field during deposition. Inclination data obtained cluster and plot around the expected inclination (±30.6°), assuming a geocentric axial dipole (GAD) for the site. With FlexIt tool reorientation, both inclination and declination in Hole U1395A show the Brunhes/Matuyama boundary (0.78 Ma; Cande and Kent, 1995) at ~66 mbsf (Figs. F8, F9). A turbidite masks the Brunhes–Matuyama transition in Hole U1395B, but it occurs between 71.9 mbsf (reversed polarity) and 67.7 mbsf (normal polarity). Based on inclinations obtained from the measurement of discrete samples in conjunction with declination data obtained from entire cores, the transition from the Jaramillo (normal) to the Matuyama (reversed) (0.99 Ma; Cande and Kent, 1995) occurs at ~90 mbsf in both holes. A sequence of unconsolidated tephras and turbidites, severely faulted and altered sediment, and poor recovery below 100 mbsf at Site U1395B make further interpretation of polarity difficult. Sedimentation rates for the uppermost 100 m of the site are therefore on the order of 8 cm/k.y. during the Brunhes Chron, with slightly higher rates at the end of the Matuyama Chron (~11 cm/k.y.), or 9 cm/k.y. for the whole record. The four deepest discrete inclination samples may indicate a polarity change indicative of the beginning of the normal Jaramillo Chron (1.070 Ma) at ~101 mbsf (Hole U1395A) and 116 mbsf (Hole U1395B), but this needs further investigation.

Physical properties

Similar to Site U1394, the physical properties of the material retrieved at Site U1395 can be correlated to lithologic variations observed in the recovered material (Figs. F8, F9). This includes compositional variations and differences in grain size and lithification stage. Based on magnetic susceptibility data, it is possible to clearly identify volcanic material retrieved in the cores. Volcaniclastic layers and turbidites exhibit pronounced positive anomalies of as much as 2800 × 10^–5 SI; ash layers show the same behavior, but the magnitude of the signal is generally smaller, with typical values of 700 × 10^–5 to 1500 × 10^–5 SI. Hemipelagic sediment and bioclastic turbidites have generally low and relatively constant magnetic susceptibility (<350 × 10^–5 and <700 × 10^–5 SI, respectively). Variations in NGR are usually antithetic to the magnetic susceptibility signature. NGR is generally low in the retrieved volcaniclastic material (typically 3–5 cps) and relatively high in the hemipelagic sediment (around 10 cps). Bulk densities vary throughout the cored material with high values (as high as 2.0 g/cm³) in turbidites that contain dense volcanic clasts but relatively low values for bioclastic turbidites. The lowest bulk density values are observed for turbidite units containing coarse pumice clasts. Porosity ranges from ~48% to 67% and displays a weak negative trend with depth. Grain density of the hemipelagic samples has a narrow range of 2.65–2.8 g/cm³. Grain density of the pumice-rich turbidite is lower, ranging between 2.45 and 2.55 g/cm³. Generally, volcaniclastic turbidites have higher velocities (1750–1800 m/s) than hemipelagic sediment (1500–1600 m/s). P-wave velocities obtained from discrete samples of the split core generally agree with velocities obtained on the whole core. Downhole formation temperature was measured at 24.9, 34.4, and 43.9 mbsf in Hole U1395B. The temperature gradient is 98.2 ± 8.8°C/km. Using the measured thermal conductivity of 1.029 W/(m·K), with a standard error on the mean of 0.017 W/(m·K), the implied heat flow is 0.101 ± 0.009 W/m². This is the highest heat flow of all sites visited during Leg 340. The corrections to this heat flow from sedimentation and bathymetry are negligible (Manga et al., 2012).

Downhole logging

In situ measurements of geophysical properties obtained by downhole logging (Fig. F9) resulted in the differentiation of three logging units (1–3). Logging Unit 1 (85–112 mbsf) is characterized by relatively consistent downhole profiles in density, resistivity, and P-wave velocity, all of which exhibit low-amplitude variability. P-wave velocities slightly increase with depth from ~1550 m/s at the top to ~1620 m/s at the base of the unit. Logging Unit 2 (further divided into logging Subunits 2A and 2B) is generally distinguished from logging Unit 1 by a sharp decrease in gamma radiation and increases in density and resistivity, as well as a broad change in the character of the logging profile. Gamma radiation, density, resistivity, and P-wave velocity all show high-amplitude variations. The drop in gamma ray intensity, associated with an increase in density and resistivity, might be an indication for turbidites in this interval. Logging Unit 3 (163–202 mbsf) is characterized by a return to lower frequency variations in all geophysical property measurements, similar to what is displayed in logging Unit 1. P-wave velocities subtly increase with depth, with the average value being higher in this lower unit than in the upper one; this is consistent with a classic compaction trend.

Geochemistry

In addition to studies done on the retrieved sediment, headspace gas samples and pore water samples obtained from hemipelagic sediment were also analyzed. Pore water samples from turbiditic units were generally not obtained because it is not possible to collect meaningful pore water data from such permeable material. Alkalinity values increased from 3.5 mM in the uppermost two sections to a maximum of 7 mM at 52.9 mbsf before decreasing to relatively constant values of 5.4 mM from 72.7 mbsf to the deepest sample at 195 mbsf. pH values are more variable (8.0–7.1) than those observed in Hole U1394B, but no consistent pattern is observable in the data, suggesting there may be some analytical artifacts in the data. Ammonium concentrations increased from 0.1 mM in the uppermost sample to 1.1 mM at 72.7 mbsf and only increased gradually to 1.2 mM at 185 mbsf. These values are lower than those observed in Hole U1394B and are consistent with the greater water depth of Site U1395, which results in greater oxidation of the organic matter before it reaches the seafloor. Calcium concentrations are only slightly lower than bottom water values in samples from the uppermost 106 m of the hole but show an increase to higher values toward the deepest sample (195 mbsf) (Fig. F9). In contrast, magnesium concentrations show a distinct decrease at the same depth interval. This simultaneous increase in calcium and decrease in magnesium is typical for pore water influenced by water-rock interaction processes with basaltic glass. Hence, it is possible that the covariation in calcium and magnesium concentrations in the deeper section of Hole U1395B may reflect a higher basaltic component in the volcanogenic material at this horizon. Potassium concentrations decrease with depth, consistent with the reaction of pore water with volcanic material. Total sulfur concentrations are slightly depleted relative to seawater and show no consistent trend with depth. Chloride concentrations fluctuate within the normal range (550–570 mM) expected for pore water obtained from squeezing carbonate sediment.

Site U1396

Background and objectives

IODP Site U1396 (proposed Site CARI-01C; 16°30.49′N, 62°27.10′W; 801 mbsl) is the most western site drilled during Expedition 340 (Fig. F3; Table T1).

The bathymetric survey for Site U1396 revealed a region bounded by a topographic high to the north and by two large canyons to the south. Site survey data indicated that this site could penetrate regular (unperturbed) seismic reflectors. The drill site is located on the topographic high to minimize any perturbations (e.g., related to turbidites). Site U1396 is located in the same area as the 5.75 m long CAR-MON 2 core taken during the Caraval cruise in 2002. Sediment recovered in the CAR-MON 2 core provides a stratigraphic record extending back ~250 k.y., as shown by δ¹⁸O chronostratigraphy. The calculated sedimentation rate (including tephra) is ~2.3 cm/k.y. (Le Friant et al., 2008). The recovered core also contained material from several explosive Plinian eruptions, which had not previously been identified on land (Le Friant et al., 2008).

The objective for Site U1396 was to characterize the eruptive history of Montserrat. Volcanism started on Montserrat at ~2.6 Ma at Silver Hills and moved to Centre Hills between 0.5 and 1.0 Ma, with the youngest volcanism being centered on the Soufrière Hills–South Soufrière Hills complex (~170 ka to present) (Harford et al., 2002). With conventional coring it is only possible to retrieve samples of recent volcanic activity. Drilling to a target depth of 132 meters below seafloor (mbsf) at Site U1396 was intended to extend our knowledge of the volcanic history of Montserrat to the birth of the island at at least ~2.5 Ma. Petrologic, lithologic, sedimentologic, and geochronologic analyses of volcanic rocks and volcaniclastic material from this site are expected to date as far back as 4 Ma (assuming a sedimentation rate of 2.3 cm/k.y. from the CAR-MON 2 study) and will provide significant new constraints on the early development of volcanism on Montserrat and on the spatial and temporal distribution of volcanic activity.

Scientific results

Lithostratigraphy

Deposits cored at Site U1396 mainly comprise a series of hemipelagic sediment, tephra layers, and volcaniclastic sand (Fig. F10). Even though the nature of the cored material at this site makes division into lithostratigraphic units more difficult, five different lithostratigraphic units (Units A–E) were identified. Unit A consists of a ~40 cm thick sequence of bioclast-rich fine sand with high water content. The sand is massive and ungraded and probably represents a high-density turbidite. Unit B (~116 m thick) comprises mainly a sequence of tephra layers (~35 layers of varying thickness, more abundant below 90–95 mbsf) intercalated in the hemipelagic background sedimentation. Hemipelagic sediment dominates the middle part of this unit. However, there may be many more layers of cryptotephras (not identifiable by standard visual core description methods) embedded in the hemipelagic mud. The tephra layers vary in thickness (mostly <5 cm; a few >10 cm) and are generally normally graded. The upper and lower layers of this unit contain a poorly sorted, massive, medium sand–sized mixture of bioclastic and volcaniclastic particles; the two occurrences of this mixture are interpreted as turbidite sequences. Isolated pebble-sized volcanic clasts are observed in the hemipelagic mud at a few locations. Unit C is ~6 m and consists of massive medium–coarse volcaniclastic sand that is mainly andesitic in composition (85%) within a finer matrix consisting of mineral particles. Unit D (122.0–123.9 mbsf) comprises a distinctive sequence of unusually coarse (commonly up to centimeter-scale clasts) pinkish breccias. This unit is composed of five fining-upward units with well-sorted intervals of pebble-sized clasts (as large as 2 cm), with little or no sand or mud-sized matrix material. Massive layers of fine sand or silt (1–5 cm thick) separate these normally graded intervals. Unit E (~16 m thick) also consists of a series of mainly well sorted tephra layers intercalated with the hemipelagic background sediment.

Thirty samples were taken to define the mineralogical composition and carbonate content of the cored material. Even though the number of tephra layers sampled at this site is high, no purely volcanic samples were obtained. In contrast to previous sites, high Mg-calcite is only present in one section (340-U1396C-6H-2). All other carbonate-rich layers contain pure calcite and aragonite in variable proportions, with calcite generally dominating the assemblage. Clay minerals are ubiquitous at this site, with smectite and kaolinite present in all samples and glauconite commonly identified. Halloysite may be present in some samples, but the spectra are not clear enough to be certain. A large bulge beneath the main peaks in some of the volcanic-rich samples suggests that significant amounts of volcanic glass are present in some of the tephra layers. CaCO₃ and organic carbon abundances indicate that the retrieved sediment is largely a mixture of carbonate-rich hemipelagic sediment with carbonate and low organic carbon volcanogenic material delivered by volcanic fallouts. The highest observed CaCO₃ concentration is 72%, with most samples much lower, suggesting that volcanic material is dispersed throughout the cores even though it is not necessarily visible to the naked eye.

Paleontology and biostratigraphy

Based on the biostratigraphic studies done on Site U1396 calcareous nannofossil and planktonic foraminiferal datums, the cored material could be assigned a late Pleistocene to early Pliocene age. Nannofossil preservation was generally good to moderate in the core catcher samples analyzed at this site. Samples obtained from ~6 to ~35 mbsf yielded a nannofossil assemblage typical for the Pleistocene with, for example, small Gephyrocapsa sp., Helicosphaera hyalina, Pseudoemiliania lacunosa, Gephyrocapsa caribbeanica, and Crenalithus doronicoides. The interval between ~44 and ~54 mbsf yielded a characteristic late Pliocene assemblage with abundant Discoaster brouweri and common Calcidiscus macintyrei in addition to Discoaster surculus and Hayaster perplexus. Between ~64 and ~91 mbsf the observed assemblages are characteristic for the early Pliocene with a variety of Discoaster species, such as Discoaster pentaradiatus, D. surculus, D. brouweri, Discoaster asymmetricus, Discoaster tamalis, Discoaster variabilis, and Discoaster challengeri. From ~100 mbsf to the bottom of the site, the retrieved samples contained Sphenolithus abies/neoabies and Reticulofenestra pseudoumbilica, which are indicative of the early Pliocene Zone CN11, Subzone CN11a S. neoabies.

Every planktonic foraminiferal biozone (PT1b, PT1a, PL6, PL5, PL4, PL3, PL2, and PL1) from Quaternary to the early Pliocene was recorded in the material deposited at Site U1396, and many different datums were observed over this 135 m interval: Globorotalia flexuosa (0.07–0.40 Ma), Globorotalia tosaensis (T 0.61 Ma), Globorotalia exilis (T 2.1 Ma), Globigerinoides extremus (T 2.1 Ma), Globorotalia miocenica (T 2.39 Ma), Globorotalia pertenuis (T 2.60 Ma), Globorotalia multicamerata (T 2.99 Ma), Sphaeroidinellopsis seminulina (T 3.16 Ma), Pulleniatina primalis (T 3.65 Ma), Globorotalia margaritae (T 3.84 Ma), and Globigerina nepenthes (T 4.36 Ma). Though several more first appearance datums are calibrated through this interval as secondary datums, when compared against the datums listed above they appeared to be largely unreliable as age determinations at this site, likely due to regional differences, and so were not used.

Paleomagnetism

The magnetostratigraphic record obtained from the material cored at Site U1396 is in excellent accordance with biostratigraphic observations. The FlexIt orientation tool was deployed with all cores from Holes U1396B and U1396C and 12 of the 15 cores from Hole U1396A. Declination can therefore be corrected to true north for most of the site. The recorded declination data show sixteen 180° shifts in declination in the longer U1396C record and fifteen in U1396A (Fig. F10). Using the geomagnetic polarity timescale (GPTS) of Cande and Kent (1995), nine periods of normal polarity and nine periods of reversed polarity can be identified for this site. The earliest polarity reversal we see in Hole U1396A is the beginning of Chron C3n.1n (4.29 Ma) at 129.4 mbsf, giving this hole a basal age of 4.29–4.48 Ma. The longer Hole U1396C record contains the end of Chron C3n.2n at 4.48 Ma, giving this hole a basal age of 4.48–4.62 Ma. Using a linear approach in conjunction with the depths of the dated reversals, an age-depth model indicates an average sedimentation rate at Site U1396 of ~3.1 cm/k.y. However, sedimentation rates vary over the observed depth interval cored at this site. Pliocene sedimentation rates are on the order of 4 cm/k.y., whereas Pleistocene rates are ~1.7 cm/k.y. and rates from the base of the core to the beginning of the Gauss Chron (3.58 Ma) are ~5.3 cm/k.y. Normalization of the NRM by magnetic susceptibility indicates good potential for construction of a relative paleointensity record for Site U1396, which should allow for greater constraint of ages in between the GPTS defined reversal horizons.

Physical properties

Physical properties data obtained for Site U1396 reflect the different material recovered relatively well (Fig. F10). Magnetic susceptibility usually increases in areas where volcanic material was recovered, whereas NGR decreases. Bulk density obtained from whole cores shows no systematic trend with depth or changes in lithology. The same is true for measured P-wave velocities on the whole cores. Discrete measurements of P-wave velocity show higher velocities for the volcanic layers (1650 to >1800 m/s) than for the hemipelagic background sediment (1550–1650 m/s). Shear strength measurements show a clear linear trend that increases with depth. Within this linear trend, there are a few anomalously low values at 85, 115, and 130 mbsf. Porosity data obtained from discrete measurements range from 54% to 70% and show no clear depth trend. Because normally compacted sands do not typically have porosities >50%, we suggest that the anomalously high porosities we observe in sandy sediments at Site U1396 may result from reworking of the sediment during core recovery and splitting. Bulk density values obtained from discrete samples range from 1.45 to 2.00 g/cm³; grain density ranges between 2.65 and 2.80 g/cm³. Formation temperature was measured at 24.6, 34.1, 43.6, and 53.1 mbsf in Hole U1396A and at 55.9 and 103.4 mbsf in Hole U1396C. The temperature gradient is 69.3° ± 1.5°C/km and, using the measured thermal conductivity of 1.04 W/(m·K), with a standard error on the mean of 0.01 W/(m·K), the implied conductive heat flow is 72 ± 2 mW/m². Because this site sits on a submarine ridge, this heat flow underestimates a conductive heat flow by 2%; sedimentation has a negligible effect on heat flow (Manga et al., 2012).

Geochemistry

Pore water from the hemipelagic sediment was analyzed, as well as headspace gases. Samples for headspace analyses were taken at 15 depths throughout Hole U1396A. The uppermost sample (from Section 340-U1396A-1H-3) had a methane concentration of 3.6 ppm, but all other samples had levels between 2.1 and 2.6 ppm. No higher hydrocarbons were detected. Samples for pore water extraction were taken from every core in Hole U1396C. Alkalinity values are generally low (<1.5 mM) throughout the hole. pH values are generally lower (7.6–7.1) than those at Sites U1394 and U1395, but no consistent pattern is observable in the data. Ammonium concentrations are much lower than at the previous two sites. These two observations may be related to the fact that Site U1396 is located at shallow water depths on a basement high with strong bottom currents. This effect tends to winnow out the finer grained, more reactive organic matter and leads to less intense organic carbon–driven diagenesis. Alternatively, the results may suggest removal of these pore fluid components through precipitation and ion exchange reactions. Calcium concentrations are consistently higher than bottom water values in samples from throughout the hole, and magnesium concentrations are consistently lower than seawater concentrations (Fig. F10). These features are commonly seen in deep sediment pore water as a result of alteration of basaltic glass and suggest that many of the tephra layers observed in the core may have a basaltic composition. This hypothesis is supported by potassium concentrations, which are also lower than seawater. Overall, ΣS concentrations are slightly depleted relative to seawater but do not show a consistent trend with depth. Chloride concentrations fluctuate within the normal range (550–570 mM) expected for pore water obtained from squeezing carbonate-rich sediment.

Site U1397

Background and objectives

IODP Site U1397 (proposed Site CARI-10B; 14°54.41′N, 61°25.35′W; 2482 mbsl) is located west of Martinique (Fig. F11; Table T1). The bathymetric survey for Site U1397 revealed a region with a topographic high bound by large canyons. Site survey seismic data indicated that this site could, in the upper part, penetrate regular (unperturbed) sedimentary reflectors, whereas in the lower part some chaotic reflectors are visible. The drill site is located on the topographic high to try to avoid perturbations. Site U1397 is located very close to Core CAR-MAR 4 (7 m long) taken during the Caraval cruise in 2002. The CAR-MAR 4 core provides a sedimentary record that extends to ~32 ka, as determined by δ¹⁸O chronostratigraphy. The sedimentation rate (including tephra) is ~20 cm/k.y. (Boudon et al., submitted). Correlating the tephra sampled in the core to onshore deposits of the Montagne Pelée Volcano shows that a significantly greater number of tephra layers are deposited in the marine environment than have been identified during onshore studies (e.g., 25 tephra layers were identified in the core between 5 and 15 ka, whereas only 10 magmatic events were previously recognized in onshore studies).

The objective for Site U1397 was to characterize the eruptive history of Martinique and the chaotic units appearing in the seismic profiles of this site. The cores retrieved will significantly improve our understanding of the eruptive history of Martinique in space and time, as we plan to sample material reaching back >1 m.y. (assuming a sedimentation rate of 20 cm/k.y. and a total target depth of 314 mbsf). We expect to identify and date layers related to the Montagne Pelée and Pitons du Carbet Volcanoes and to sample the region related to the transition of volcanism from the Pitons du Carbet and Mont Conil Volcanoes to the Montagne Pelée Volcano. The end of volcanic activity at the Pitons du Carbet and Mont Conil Volcanoes (~0.3–0.5 Ma) precedes the beginning of the Montagne Pelée activity. We want to test the hypothesis that more mafic and denser magma was erupted for a period of several thousand years following edifice collapse until a new lava cone reached sufficient volume to erupt more evolved lavas (Pinel and Jaupart, 2000; Boudon et al., 2007). This site could also contain tephra from Dominica volcanoes, which will be distinguished on the basis of geochemistry and microtextural characteristics (Machault, 2008). Volcanism on Dominica has been dominated by andesitic to dacitic eruption products since the Pleistocene (Lindsay et al., 2005c).

Scientific results

Lithostratigraphy

A continuous stratigraphic record was only retrieved for the uppermost 120 m at this site because of generally poor recovery below this depth (Figs. F12, F13). Sediment retrieved at this site was divided into eight lithostratigraphic units (Units A–H). Similar to the other sites, each unit consists of various combinations of hemipelagic mud, volcaniclastic or mixed (volcaniclastic-bioclastic) turbidites, and various tephra layers. Generally, unit boundaries and the material cored are similar in both holes, except that a higher proportion of turbidites and a lower proportion of tephra are observed in some units in Hole U1397B compared to those in Hole U1397A. It is likely that most of the missing tephras were eroded during the emplacement of turbidites. Boundaries for each of the lithostratigraphic units are defined by abrupt or gradational changes in the abundance of lithologies, distinctive marker horizons, different mineralogical compositions of tephra, and/or unusually thick turbidites. Unit A (0–28 mbsf in Hole U1397A and 0–26 mbsf in Hole U1397B) is composed of a thick sequence of hemipelagic sediment with interbedded tephra and volcaniclastic layers. The tephra layers, of which there are at least 200, are well sorted and either massive or normally graded. The few turbidites observed in this unit are poorly sorted. Unit B (28–53 mbsf in Hole U1397A and 26–53 mbsf in Hole U1397B) is composed of tephra layers and volcaniclastic turbidites intercalated in hemipelagic mud. The proportion of turbidites is higher than that found in Unit A. Turbidites are normally graded and contain variable amounts of fresh pumice. The matrix of the turbidites is mainly composed of crystals and very low proportions of carbonates and lava clasts. Most of the tephra layers are dark and fine grained and are frequently normally graded. Unit C (53–77 mbsf in Hole U1397A and 53–78 mbsf in Hole U1397B) is divided into two subunits (C-1 and C-2). Subunit C-1 is dominated by thick turbidite sequences of mixed (bioclastic-volcaniclastic) composition. Crystals, massive lava fragments, and pumice particles (sometimes in higher proportions) make up the volcanic component of these turbidites. Hemipelagic mud is frequently absent between turbidite layers. Subunit C-2 (<3 m thick) comprises a debris flow deposit and a section of deformed sediment. The debris flow deposit consists of very abundant deformed mud clasts and large fragments of hydrothermally altered and fresh andesitic lava. Unit D (77–91 mbsf in Hole U1397A and 78–95 mbsf in Hole U1397B) is composed of a series of volcaniclastic turbidites and a few tephra layers, which are interbedded in a hemipelagic mud. The proportion of hemipelagic sediment is very low in this unit, attesting to the erosional character of the turbidites. Unit E (91–120 mbsf in Hole U1397A and 95–150 mbsf in Hole U1397B) is composed of a series of thick massive to normally graded volcaniclastic turbidites containing a large amount of massive to poorly vesiculated lava fragments. The base of this unit is not observed, and below this unit the stratigraphy is more uncertain, as core recovery was very low. Unit F (150–168 mbsf in Hole U1397A and 150–160 mbsf in Hole U1397B) is divided into two subunits on the basis of the compaction of the sediment. Subunit F-1 is composed of a package of hemipelagic mud with a few interbedded tephra layers, whereas Subunit F-2 is composed of the same sequence of sediment, weakly compacted at the top and showing progressive lithification into mudstones toward the base. Unit G (168–230 mbsf in Hole U1397A and 160–247.5 mbsf, the bottom of Hole U1397B) is composed of mud-rich sandstone layers and semiconsolidated, highly fractured, and contorted mudstones. It contains abundant lava clasts, few pebbles, and a larger block composed of andesitic lava containing large phenocrysts of amphibole and quartz. Similar lava is generated by the Pitons du Carbet Volcano, south of Montagne Pelée, and is unique to the area of Martinique and Dominica. The period of activity that generated this type of magma is dated at ~330–350 ka (Germa et al., 2011; Samper et al., 2008). Unit H (230–259.6 mbsf) is only represented in Hole U1397A. Unit H consists of heavily bioturbated hemipelagic mud. A few layers of bioclastic sandstone are interbedded within the mudstone.

Forty-four samples were taken to characterize the mineralogy of the volcanic material cored and the carbonate content. The volcanic material retrieved contains mainly plagioclase, hornblende, quartz, and amphibole. Hornblende appears to be more alkali rich than observed in samples from around Montserrat. Clay minerals are ubiquitous throughout the hole and are also more abundant than in samples from the Montserrat sites. The dominant clay minerals are smectite, kaolinite, and glauconite. At the base of Hole U1397A, the abundance of clay minerals (mainly smectite) is especially high, and dolomite is also present in significant quantities, possibly reflecting the presence of hydrothermal alteration products. CaCO₃ concentrations are lower than those found in the sites around Montserrat, and the main carbonate minerals identified are calcite with minor aragonite. This combination likely reflects the greater water depth at this location and the absence of any significant aragonite preservation.

Paleontology and biostratigraphy

The nanno- and microfossil content of the sediment described above are persistently reworked, and many samples contain poorly preserved shallow-water reef benthic foraminifers and coral fragments. Generally, the sediment contained low abundances of calcareous nannofossils and planktonic and benthic foraminifers with varying levels of preservation. Where obtained, biostratigraphic dates were generally nonsequential; however, an overall trend to older material with increasing depth is observed. Calcareous nannofossils and planktonic foraminifers show that Site U1397 contains many levels of reworked sediment from the upper Miocene to upper Pliocene amidst a background of upper Pleistocene sedimentation. Overall, only a few datum species (Globigerinella calida, Globorotalia flexuosa, and Emiliania huxleyi) could be used as an age constraint for the cored material. The resulting age model resolves an age younger than 220 ka for the top ~25 mbsf, younger than 250 ka from ~50 to ~100 mbsf, younger than ~350 ka from 100 mbsf to nearly the base, and ~400 ka at the bottom of this site. It should be noted that these ages are only a maximum age estimate and that any constraint on the youngest material is inappropriate given the extensive reworking of sediment.

Paleomagnetism

Generally, the retrieval of a magnetostratigraphic record for this site was as complicated as the retrieval of a biostratigraphic record because of the nature of the cored material and recovery. Using the detailed core description logs, only data measured on identifiable hemipelagic sediment layers were used for interpretation. These layers were highly discontinuous at Site U1397, particularly below ~55 mbsf. Shallower than ~55 mbsf, inclination values obtained on discrete samples show scattered but positive inclination, clustering around the expected GAD inclination. Declination shows little variation, suggesting that all sediment and tephra to a depth ~55 mbsf was deposited in the Brunhes Chron (<780 ka). Below this depth the record becomes increasingly discontinuous, making confident interpretation of ages based solely on paleomagnetic data difficult.

Physical properties

The physical properties of the material retrieved at Site U1397 can generally be correlated to the lithologic variations observed throughout the cored material (Figs. F12, F13). Bioclastic and volcaniclastic turbidites and thick tephra layers can be distinguished from background sedimentation (hemipelagic mud) by most of the physical proprieties. Magnetic susceptibility data show large variations, with maximum values (6880 × 10^–5 SI) more than twice as high as those obtained from measurements at the other sites. Peaks in magnetic susceptibility values correlate with tephra layers and volcaniclastic turbidites. Measured bulk densities increase slightly with depth, whereas NGR data show no consistent downhole trend. P-wave velocity ranges between 1400 and 1750 m/s with no significant downhole increase. All three of these properties have a sharp boundary at depths that correspond to the base of turbidites. The shear strength of the cored sediment increases with depth (1 kPa/m) for the uppermost ~55 mbsf at Site U1397. No shear strength measurements could be performed in the interval between ~55 and 65 mbsf because of the coarse nature of the retrieved sediment (mainly sand). Between 65 and 80 mbsf, shear strength increases as high as 200 kPa; it then decreases from 80 to 95 mbsf. The interval between 95 and 150 mbsf was again not favorable to measure shear strength. Between 150 and 180 mbsf shear strength is quite variable, with values ranging from <50 to >450 kPa, reflecting the variable nature of the sampled sediment and likely variable consolidation states. Porosity data show, as was observed at Site U1396, no consistent trend with depth. Porosity ranges from ~40% to 68%. Bulk density ranges from 1.55 to 2.40 g/cm³ and shows a clear negative correlation with porosity. The dark-colored volcaniclastic turbidites have systematically higher bulk densities (1.75–2.40 g/cm³) than the other retrieved sediment. Grain density ranges between 2.48 and 3.17 g/cm³, with hemipelagic sediment showing grain densities between 2.6 and 2.85 g/cm³. Formation temperature was measured using the APCT-3 at 36.5, 46.0, and 55.5 mbsf in Hole U1397A and 25.6, 35.1, and 61.3 mbsf in Hole U1397B. The temperature gradient is 70.0° ± 8.8°C/km. Using the thermal conductivity of 1.028 W/(m·K), with standard error on the mean of 0.022 W/(m·K), the implied conductive heat flow is 72 ± 9 mW/m². The bathymetry of this site lowers the near-surface (measured) heat flow by 4%, and the high sedimentation rate of this site can lead to heat flow being underestimated by as much as 4% (Manga et al., 2012).

Downhole logging

In situ measurements of geophysical properties obtained by downhole logging in Hole U1397B should be treated with caution because of the large diameter of the borehole. An oversized borehole such as Hole U1397B can make centralization and eccentralization of the tools in the borehole difficult, with gamma ray and FMS measurements being the most significantly affected. Measurements of electrical resistivity, magnetic susceptibility, and P-wave velocity are less affected, and general trends and relative changes displayed by those measurements should be reliable.

Four logging units were identified based on specific characteristics observed across the physical properties measured. Logging Unit 1 (85–90 mbsf) is characterized by relatively consistent values of resistivity and gamma radiation and average values of P-wave velocity (~1650 m/s). Magnetic susceptibility decreases with depth. Logging Unit 2 (90–127 mbsf) is characterized by four intervals that exhibit increasing resistivity and P-wave velocity with depth. The boundaries of these intervals are marked by distinct changes in magnetic susceptibility (local peaks superimposed on the general decreasing trend with depth). Logging Unit 3 (127–185 mbsf) shows a return to less variable resistivity and P-wave velocity values. This logging unit is divided into two subunits (logging Subunits 3A and 3B) based on subtle changes in the character of the recorded geophysical properties, of which magnetic susceptibility is the most distinctive. The amplitude of magnetic susceptibility variations is much higher in logging Subunit 3A than in logging Subunit 3B. In addition, P-wave velocity is slightly higher in logging Subunit 3B (average = ~1760 m/s) than in logging Subunit 3A (average = ~1710 m/s). Logging Unit 4 (185 mbsf to base of the hole) is characterized by higher values of resistivity and magnetic susceptibility than those found in logging Unit 3. P-wave velocity is also higher in this unit (average = ~1900 m/s), completing the downhole trend of increasing P-wave velocity.

Geochemistry

Samples for headspace gas analysis were taken from 18 depths throughout Hole U1397A. Samples from the uppermost 76 m tend to have slightly higher methane concentrations (3.1–4.4 ppm) than those from 94 to 266 mbsf (2.3–3.7 ppm). No higher hydrocarbons were detected. Pore water alkalinity values increase with depth in the upper part of the sediment at this site and reach a maximum of 5.1 mM between 23 and 46 mbsf before decreasing to 3.9 mM in the deepest samples (164–182 mbsf). pH values vary between 7.3 and 8.2, but no consistent pattern is observable in the data. Ammonium concentrations are lower than those at comparable sites around Montserrat (Sites U1394 and U1395); the lower concentrations likely reflect the greater water depth of this site. The shape of the ammonium profile is similar to that of the alkalinity profile, suggesting that diagenetic processes in the sediment column dominate both. Calcium concentrations decrease from the seawater value to 9.1 mM at 23 mbsf and then increase to 11.0 mM in the deepest sample (182 mbsf) (Fig. F13). Magnesium concentrations (which scatter around values slightly higher than seawater) and potassium concentrations (which are higher in the uppermost 75 mbsf and show a weak trend to lower values between 164 and 182 mbsf) suggest that alteration of volcanic matter does not play a dominant role in defining major element pore water concentrations. ΣS concentrations decrease from the seawater value to 26 mM at 43 mbsf and then increase to near seawater concentrations in the deepest samples. Chloride concentrations are within the normal range (560–570 mM) expected for pore water obtained from squeezing carbonate-rich sediment.

Site U1398

Background and objectives

IODP Site U1398 (proposed Site CARI-09B; 14°16.70′N, 61°53.34′W; 2935 mbsl) is located west of Martinique (Fig. F3; Table T1). The objective for this site was to characterize the sedimentation processes in the backarc Grenada Basin. We planned to drill through hemipelagic sediment and turbidites and retrieve a complete sedimentation record to ~264 mbsf. Site survey data showed that we could penetrate sedimentary reflectors indicative of the deposition of hemipelagic sediment and turbidites. With the recovered material we hope to identify the turbidites related primarily to debris avalanche deposition. One focus is to evaluate whether submarine debris avalanches can generate voluminous turbidites long after their emplacement and, if so, how far such turbidites can travel. We also expect to improve the reconstruction of the postcollapse eruptive activity of Pitons du Carbet (Boudon et al., 2007). This will provide better constraints on the transition of activity between the Pitons du Carbet and Montagne Pelée Volcanoes. Finally, we expect to sample turbidites with volcanic material coming from Dominica (e.g., Roseau tuff).

Scientific results

Lithostratigraphy

Generally, the upper parts of both holes at this site are dominated by volcaniclastic turbidites, whereas the lower portions are composed of various combinations of hemipelagic sediment with intercalated volcaniclastic turbidites and tephra (Figs. F14, F15). The retrieved sediment was divided into seven lithostratigraphic units (Units A–G). The uppermost 70 cm of Unit A (0 to ~40 mbsf) is composed of hemipelagic mud; below this depth Unit A is composed of a series of thick volcaniclastic turbidites, consisting of massive, normally graded sand-sized minerals, lava particles, and detrital carbonates interrupted by thin layers of hemipelagic mud. Abundant pumice clasts are common throughout the entire unit. The upper part of Unit B (~40 to ~57 mbsf) consists of hemipelagic sediment with interbedded thin tephra layers, whereas the lower part is composed of a succession of massive normally graded turbidite sequences, which can be as thick as 6 m. Turbidites occasionally display compositional laminations, grain-size layering, and parallel stratification in the upper part of each layer. Unit C (~57 to ~80 mbsf) consists of hemipelagic mud interbedded with multiple thin tephra layers and thin turbidites. The turbiditic sequences, exhibiting mainly normal grading, generally contain pumice clasts and hemipelagic clay. Unit D (~80–104 mbsf in Hole U1398A and ~80–99 mbsf in Hole U1398B) is composed of a succession of massive turbidites that are a few meters thick. The turbidites, often displaying normal grading, are separated by hemipelagic sediment interbedded with thin tephra layers. The upper of two distinctive pink-colored ash layers forms the lower boundary of Unit D. Unit E (104–115 mbsf in Hole U1398A and 99–115 mbsf in Hole U1398B) is characterized by multiple tephra layers. It also contains a few turbidites that are generally <1 m thick, interbedded with hemipelagic sediment. Two pinkish, 1 cm thick glassy ash layers are present in the upper half of Unit E. The top of Unit F (115–171 mbsf), only fully recovered in Hole U1398B, is composed of a 3 m thick debrite followed by a succession of thick massive turbidites. Below the sequence of massive turbidites, Unit F comprises a sequence of intercalated multiple thin tephra layers and small-scale turbidites. Unit G (171–260.5 mbsf in Hole U1398A and 171–254.8 mbsf in Hole U1398B) mostly comprises well-lithified, heavily bioturbated hemipelagic mud. This unit occasionally contains interbedded volcaniclastic sand layers. A whitish to pinkish colored, 1 cm thick glassy ash layer occurs at 232 mbsf in Hole U1398A and 246 mbsf in Hole U1398B.

XRD data obtained from discrete samples throughout the cores show that quartz and plagioclase minerals dominate the volcanic material, whereas the marine sediment is dominated by calcite and lesser amounts of aragonite. Amphibole is less frequently present than in the cores obtained from previous sites. Smectite, kaolinite, and, to a lesser extent, glauconite are also ubiquitous. Clay abundance increases with depth. Pyrite has often been observed in the cored material that is rich in volcanic particles but could not be identified by XRD. Calcium carbonate concentrations are highly variable and are generally lower in intervals with higher proportions of volcanic material. Maximum concentrations are ~35%, reflecting the greater proportion of terrestrial clay minerals and possibly the absence of significant aragonite preservation.

Paleontology and biostratigraphy

Using calcareous nannofossil as well as planktonic foraminiferal datums, the cored material could be assigned to the upper Pleistocene, indicating extremely high sedimentation rates. However, as observed in the cored material of previous sites, reworking of much older (early Pleistocene and late Pliocene) material is evident in several of the studied samples. This is consistent with the shallow-water benthic foraminifers, fragments of shells and corals, pteropods, heteropods shells, otoliths, and sponge spicules (Demospongiae) observed throughout the many of the samples examined. The nannofossil species observed at this site (typically prevalent: Emiliania huxleyi, Gephyrocapsa oceanica, Gephyrocapsa caribbeanica, Gephyrocapsa parallela, Ceratolithus cristatus, and Ceratolithus telesmus) are characteristic of upper Pleistocene sediment. Thus, the entire sequence was placed in Zone CN15, E. huxleyi, which has a maximum age of 0.25 Ma. The presence of Miocene to Pliocene nannofossil species throughout much of the sampled sediment indicates extensive reworking of the sediment retrieved at this site. Planktonic foraminifers were present in all samples, although some were found at very low abundances, possibly because of the high volume of volcanic material. In samples with abundant specimens, the assemblage of planktonic foraminifers was diverse but dominated by Globigerinoides ruber (white and pink), Globigerinoides sacculifer, and Neogloboquadrina dutertrei (dextral). Other abundant species include Globorotalia truncatulinoides and Globorotalia tumida. The fauna does not change significantly throughout the section recovered at Site U1398, and all species present are indicative of warm subtropical waters. The presence of Globigerinella calida (B 0.22 Ma) at the base of this site dates the sediment to younger than 0.22 Ma, within the Pleistocene. Marker species characteristic of early Pleistocene and late Pliocene ages were also found, but they simply reinforce the reworked nature of the deposited sediment. Based on the occurrence of Cibicides wuellerstorfi and Pyrgo murrhina, a bathyal paleodepth was interpreted.

Paleomagnetism

Generally, the magnetostratigraphic record obtained from the cored material is in accordance with biostratigraphic observations, despite creation of the stratigraphic record being complicated by discontinuous retrieval of hemipelagic sediment throughout the holes at Site U1398. Between 0 and ~170 mbsf at this site, all inclination data show scattered but positive inclination, clustering around the expected inclination as predicted by a GAD (±27°). Declination agrees, showing little variation, and suggests that sediment shallower than 170 mbsf was deposited within the Brunhes Chron and is younger than 780 ka (Cande and Kent, 1995). Recovery of sediment deeper than 170 mbsf using the XCB resulted in core rotation and magnetic overprinting, restricting polarity interpretation to discrete measurements of inclination at roughly 10 m intervals. Inclinations are generally shallower than would be expected based on the GAD at this location; however, without declination data to reinforce these shallow inclination data, interpretation of polarity is difficult. Some sections of the core show evidence for postdepositional deformation; however, this evidence cannot account for all the observed negative inclination intervals. If these consistently negative inclination values show true geomagnetic behavior, it would suggest that sediment below ~170 mbsf was deposited during the Matuyama Chron; however, this is not consistent with the biostratigraphic data and requires further postcruise analysis.

Physical properties

Similar to the other sites, the physical properties of the material retrieved at Site U1398 can be correlated to the lithologic variations observed in the recovered material (Figs. F14, F15). Magnetic susceptibility varies between 1000 × 10^–5 and 2500 × 10^–5 SI (maximum = 6700 × 10^–5 SI) in the sediment containing considerable amounts of volcanic clasts (mainly andesitic in composition) and is mostly below 700 × 10^–5 SI in the hemipelagic sediment. Usually, magnetic susceptibility also decreases with decreasing grain size in normally graded volcaniclastic layers. NGR varies inversely with magnetic susceptibility. It shows count rates as high as 35 cps in the hemipelagic sediment and count rates as low as 8 cps in the volcaniclastic sediment. P-wave velocities vary between 1650 and 1850 m/s in the volcaniclastic sediment and between 1500 and 1600 m/s in the hemipelagic sediment. Bulk density and P-wave velocity decrease with grain size in normally graded turbiditic sequences. Shear strength measurements were not performed in the uppermost 40 and 60 mbsf of Holes U1398A and U1398B, respectively, because of the presence of sandy and gravelly sediment. Below these depths, although the shear strength measurements show considerable scatter, a general trend of increasing shear strength is observed. Porosity in the hemipelagic sediment ranges between 60% and 75%, and, as at the other sites, no trend with depth was observed. Porosity in the volcaniclastic deposits varies between 39% and 67%; however, calculated porosity values in volcaniclastic sediment may be inaccurate due either to pore water draining or grain reorganization during recovery. Bulk density of the hemipelagic sediment ranges between 1.46 and 1.77 g/cm³. Volcaniclastic sediment has bulk densities as high as 2.2 g/cm³. Grain density of the hemipelagic sediment and volcaniclastic sand shows a range between 2.6 and 2.8 g/cm³. Temperature was measured using the APCT-3 at 45.6 and 60.4 mbsf in Hole U1398A and 26.5, 58.1, and 73.8 mbsf in Hole U1398B. The temperature gradient is 57.4° ± 5.0°C/km. Using the measured thermal conductivity of 1.034 W/(m·K), with standard error on the mean of 0.012 W/(m·K), the implied conductive heat flow is 59 ± 5 mW/m². No bathymetric correction is needed, and sedimentation may lower the measured near-surface heat flow by as much as 4% (Manga et al., 2012).

Geochemistry

Twenty-three headspace samples were analyzed for gas content. Methane concentrations are very low (a few parts per million) in the upper parts of the sediment retrieved from Site U1398 but increase rapidly below 180 mbsf to a maximum value of 4700 ppm at 240 mbsf. Despite these elevated methane levels, concentrations of the higher hydrocarbons remained close to detection limits, with between 0.4 and 1.4 ppm ethane and ethene measured in seven samples. Because of the coarse-grained nature of the sediment, it was not possible to take any pore water samples in the uppermost 60 mbsf at this site. Hence, the uppermost pore water data come from 62.5 mbsf. At this point, pore water alkalinity values are close to 10 mM and remain at this level to 150 mbsf. Alkalinity then decreases to 5.9 mM at 254 mbsf. Ammonium concentrations increase steadily from 0.8 mM in the shallowest samples to ~1.6 mM in the deepest sample. Calcium concentrations decrease from 4.8 mM at 62.5 mbsf to 3.4 mM at 86 mbsf and then remain relatively constant with an increase to 10.9 mM in the deepest sample (Fig. F15). Magnesium concentrations also gradually decrease from 51 mM in the shallowest sample to 44.4 mM at the base of the hole. Chloride concentrations show a consistent increase from close to the seawater value in the shallowest sample to 674 mM at 254 mbsf. Even the shallowest sample has sulfur concentrations that are less than half the seawater level, and then concentrations fall below 10 mM at 65 mbsf and reach our detection limit by ~160 mbsf. Overall, data are consistent with diagenetic processes controlled by organic carbon oxidation and alteration of volcanic material. The increase in chloride with depth may reflect hydration of clay minerals.

Site U1399

Background and objectives

IODP Site U1399 (proposed Site CARI-08B; 14°23.24′N, 61°42.69′W; 2900 mbsl) is located west of Martinique (Fig. F11; Table T1). The objective for Site U1399 was to characterize the processes accompanying debris avalanche emplacement and associated erosion. The seismic and bathymetric surveys for Site U1399 revealed that this site is located on one of the main chaotic deposits and that coring at this site could retrieve volcanic and biogenic sediment with intercalated, large, chaotic unit (interpreted as debris avalanche Deposit 1) (Le Friant et al., 2003; Boudon et al., 2007). In detail, we hope to characterize and quantify the erosional processes of the upper sedimentary layers deposited in the Grenada Basin associated with such mass transport processes and their subsequent incorporation into the flow. Finally, we will compare the characteristics of the deposits from Dominica and Martinique to constrain possible differences in erosional capability and mobility. Sediment above Deposit 1 will be used to better constrain the age of the mass-wasting event.

Scientific results

Lithostratigraphy

Sediment cored at Site U1399 is dominated by a combination of hemipelagic mud with interbedded tephra and volcaniclastic turbidites, as well as various types of deformed sedimentary intervals that occur at different depths (Figs. F16, F17). Eight lithostratigraphic units (Units A–H) were defined based either on characteristic changes throughout the cored material or distinct marker layers. Unit A (0–24 mbsf in Hole U1399A and 0–12 mbsf in Hole U1399B) is mainly composed of hemipelagic mud with abundant interbedded tephra layers. In Hole U1399A, several small turbidites are also interbedded with hemipelagic mud, whereas only one turbidite could be identified in Hole U1399B. Most tephra and turbidite layers contain pumice in variable abundances (5%–65%). Unit B (24–50.5 mbsf in Hole U1399A and 12–29 mbsf in Hole U1399B) is composed of a thick sequence of variably deformed hemipelagic sediment with several areas of inclined and convoluted banding. This unit also contains debris flow deposits (debrites) with a muddy sand matrix. Dispersed lava clasts and deformed tephra layers are often found within the debrites. Unit C (50.5–72 mbsf in Hole U1399A and 29–53 mbsf in Hole U1399B) consists of hemipelagic mud with interbedded tephra layers and thin turbidites (<1 m thick). The base of Unit C is composed of a 1 m thick interval of hemipelagic mud overlain by a turbidite. This basal turbidite is 8.2 m thick in Hole U1399A and 2.1 m thick in Hole U1399B. The upper part of Unit D (72–76 mbsf in Hole U1399A and 53–68.5 mbsf in Hole U1399B) is composed of deformed sediment with inclined contacts between zones of different colored mud, whereas the lower part is composed of weakly deformed hemipelagic mud with inclined green laminae. Unit E (76–112 mbsf in Hole U1339A and 68.5–102.7 mbsf in Hole U1339B) consists of a succession of alternating layers of undeformed hemipelagic mud with interbedded tephras and thin turbidites, deformed hemipelagic mud, debrites, and thick turbidites. Unit F (112–142.5 mbsf in Hole U1399A and 102.7–129 mbsf in Hole U1399B) is composed of a thick sequence of highly deformed and contorted sediment, including some turbidites and contorted tephra layers. Unit G (142.5–191.7 mbsf in Hole U1399A and 129–182.3 mbsf in Hole U1399B) is mainly composed of thick sequences of pumice-rich turbidites with interbedded hemipelagic mud containing a few tephra layers. The proportion of hemipelagic mud in this unit is low. Unit H (191.7–270 mbsf in Hole U1399A) is mainly composed of hemipelagic mud, with interbedded tephra layers and pumice-rich turbidites. The proportion of hemipelagic mud (70%) is higher than in preceding units, and tephra layers are frequently observed.

As shown by the carbonate analysis of 33 samples throughout the entire cored interval, calcium carbonate concentrations are highly variable and are lower in intervals with higher proportions of volcanic material and presumably terrestrial clay. The maximum concentration is ~35 wt%, which also partly reflects the absence of significant aragonite preservation.

Paleontology and biostratigraphy

Core catcher samples taken from Site U1399 contain calcareous nannofossils and planktonic and benthic foraminifers of varying abundances and at varying levels of preservation. Calcareous nannofossil and planktonic foraminiferal datums obtained from the cored material show that the sediments were deposited during the late Pleistocene, indicating an extremely high sedimentation rate for this site. Reworking of much older (early Pleistocene and late Pliocene) material is evident in several samples. Many of the core catcher samples from Site U1399 consist of very coarse grained material containing numerous shallow-water benthic foraminifers and fragments of shell and coral. Well-preserved pteropod and heteropod shells, otoliths, and sponge spicules (Demospongiae) were also found in some of the hemipelagic samples. The nannofossil assemblage was dominated by Gephyrocapsa oceanica, Gephyrocapsa parallela, Helicosphaera hyalina, and Emiliania huxleyi, though several samples contained obviously reworked species (the early Paleocene species, Binatholithus sparsus, for example). The assemblage of observed planktonic foraminifers was diverse but dominated by Globigerinoides ruber (white and pink), Globigerinoides sacculifer, and Neogloboquadrina dutertrei (dextral). Other abundant species include Globorotalia truncatulinoides and Globorotalia tumida. The assemblage does not change significantly throughout the site, and all species present are indicative of warm subtropical waters. Several datum species were found; however, marker species were generally not found in samples with low planktonic foraminifer abundance. Globorotalia flexuosa (0.07–0.40 Ma) and Globigerinella calida (B 0.22 Ma) were only found in low numbers. The last occurrences of these datum species are not clearly defined, and no reliable planktonic foraminiferal datum was found at the base of either hole. Many reworked specimens were found within the samples, from early Pliestocene to possible Miocene. Again, because of the lack of certain obvious species, a paleodepth estimate based on benthic foraminifers is difficult, but based on the presence of Cibicides wuellerstorfi and Pyrgo murrhina, a bathyal paleodepth is interpreted.

Paleomagnetism

Interpretation of the behavior of the geomagnetic field during the deposition of cored sediment to derive a magnetostratigraphic record is based only on the data from nondeformed intervals. This is roughly 20% of the paleomagnetic directional data obtained from Site U1399, resulting in a highly discontinuous record. Expected inclination for the site is ±27.2° assuming a GAD. Between 0 and 207.5 mbsf in Hole U1399A and in all of Hole U1399B, SRM and discrete inclination data show scattered but positive values, clustering around the expected GAD inclination. Declination also shows some scatter, but coupled with the positive inclination data it suggests all sediment was deposited under normal polarity conditions. Interpretation is severely hampered because of the lack of a continuous record, and we cannot unequivocally say that all sediment was deposited within the Brunhes chron; however, this would indicate a late Pleistocene age for the site.

Physical properties

Unlike previous sites, magnetic susceptibility data obtained from the cored material at Site U1399 show no clear variation with the material recovered (Figs. F16, F17). Only two strong peaks correlating to thick layers of coarse-grained volcaniclastic material were observed in both holes. Bulk density data scatter around an average value of 1.7 g/cm³ and generally increase with depth. Bulk density obtained from measurements of discrete hemipelagic samples ranges between 1.5 and 1.8 g/cm³, displaying a weak positive correlation with depth. Sandy samples have bulk densities as high as 2.05 g/cm³. Grain density varies between 2.65 and 2.8 g/cm³. Volcanic sand has a similar grain density compared to hemipelagic samples. Porosity obtained from the measurement of discrete hemipelagic samples ranges between 53% and 73%. Site U1399 shows a weak negative porosity-depth correlation from ~70% at the mudline to ~60% at 270 mbsf. Porosity in volcanic sand samples ranges between 40% and 50%. The porosity of the loose sand may be underestimated by as much as 20% because of draining pore water during coring, splitting, and sampling. On the other hand, reworking of sand during coring and splitting may increase porosity. NGR data distinguish between hemipelagic sediment and volcanic material, with count rates in the hemipelagic material varying between 15 and 50 cps and count rates in the volcanic material are below 15 cps. P-wave velocities obtained from hemipelagic sediment shallower than 140 mbsf range from 1500 to 1550 m/s, whereas the volcaniclastic material shows velocity values between 1650 and 1800 m/s. The shear strength of the recovered material generally increases downhole in both holes with higher values typically measured with the handheld penetrometer. Downhole formation temperature was measured using the APCT-3 at 24, 34, 43, and 53 mbsf in Hole U1399A and 25, 53, and 81 mbsf in Hole U1399B. The geothermal gradient is 65.4° ± 0.9°C/km. Using the measured thermal conductivity of 1.045 W/(m·K), with uncertainty on the mean of 0.008 W/(m·K), the implied conductive heat flow is 68 ± 1 mW/m². Sedimentation lowers the measured near surface heat flow by as much as 4%. Despite a separation of 410 m between the two holes cored at this site, all temperature measurements lie on a single line. This implies that fluid flow is not disturbing the temperature gradient.

Downhole logging

In situ measurements of geophysical properties obtained by the downhole logging operations in Hole U1399C are generally of good quality (Fig. F18). Four different logging units were identified based on specific characteristics observed across the physical properties measured, especially gamma ray, resistivity, and magnetic susceptibility. Logging Unit 1 (80–106 mbsf) is characterized by an overall increase in gamma radiation with depth from ~25 to ~50 gAPI. Magnetic susceptibility and electrical resistivity profiles are similar in character with a small net decrease with depth. At 106 mbsf, the transition from logging Unit 1 to logging Unit 2 (106–150 mbsf) is marked by a sharp decrease in gamma radiation that coincides with sharp increases in resistivity and magnetic susceptibility. Similar to logging Unit 1, logging Unit 2 shows a net increase in gamma ray with depth. Between 140 and 150 mbsf, gamma ray values are elevated; this increase is reflected in both the total gamma ray and spectral gamma ray measurements. Interestingly, this increase is not shown in the corresponding NGR data from cores recovered in Hole U1399A. Resistivity generally decreases with depth through this logging unit, with localized high-resistivity features. This trend is repeated in the magnetic susceptibility curve. Logging Unit 3 (150–181 mbsf) is characterized by higher amplitude variability in gamma ray, resistivity, and magnetic susceptibility. Similar to the transition between logging Units 1 and 2, the transition from logging Unit 2 to logging Unit 3 is marked by a stepwise decrease in gamma radiation and increases in resistivity and magnetic susceptibility. Generally, lower values of gamma radiation coincide with higher values of both resistivity and magnetic susceptibility. Logging Unit 4 (181 mbsf to total hole depth) is characterized by more regular gamma ray variations, on the order of ~15 gAPI, continuing through the uppermost 25 m of this unit, after which variations decrease in amplitude. In addition, this unit exhibits the most variable magnetic susceptibility profile in Hole U1399C, including some significant peaks, the largest of which (~205–208 mbsf) corresponds to similarly elevated values of resistivity. Check shot traveltimes obtained by seismic experiments range from a 0.128 s two-way traveltime at 87.8 mbsf to 0.279 s at the bottom of the hole (225.7 mbsf).

Geochemistry

Twenty-eight samples for headspace analyses were taken throughout the hole. Methane concentrations were only a few parts per million in all but the deepest sample (276 mbsf in Hole U1399A), which yielded a methane concentration of 690 ppm. This is slightly deeper than the zone of high methane concentrations observed at Site U1398. The major ion pore water profiles are characteristic of a deep-sea diagenetic sequence. Total sulfur concentrations gradually decrease over the same interval over which alkalinity and ammonium steadily increase. Calcium concentrations show a steady decrease with depth, reflecting precipitation of secondary carbonate (Fig. F17). Magnesium concentrations also decrease with depth, most likely caused by the alteration of volcanic material. The slight increase in chloride concentrations also reflects uptake of water into secondary mineral phases at depth. The shapes of the pore water profiles suggest that the main oxidation of organic carbon takes place in the uppermost 60 m of the sediment column. Generally, organic carbon concentrations decrease with depth but are highly scattered. The uppermost 115 m of the interval cored contain several samples with organic carbon concentrations close to 1 wt%, whereas the maximum concentration observed in the lower 155 m is ~0.7 wt%. The change in organic carbon concentrations between the upper 115 m and the lower 155 m of the sediment column may reflect a change in the input of organic carbon to the system rather than changes in preservation. There is, however, a strong caveat to this hypothesis, as the percentage of volcanic material can also vary with depth, and this may cause variable dilution of a constant input flux of organic carbon to the sediment.

Site U1400

Background and objectives

IODP Site U1400 (proposed Site CARI-07C; 14°32.58′N, 61°27.55′W; 2745 mbsl) is located west of Martinique (Fig. F11; Table T1). Site U1400 was dedicated to the study of debris avalanche emplacement and associated erosional processes. The evolution of the active Montagne Pelée Volcano is characterized by three major flank-collapse events (~0.1 m.y., ~25,000 y, and ~9000 y ago) that systematically destroyed the western flank of the volcano (Le Friant et al., 2003; Boudon et al., 2005, 2007). The volume of material displaced by these collapses varies from 2 to 25 km³, with the debris avalanches depositing into the Grenada Basin. The Pitons du Carbet Volcano experienced a sector collapse 0.3 m.y. ago (Boudon et al., 1992, 2007; Samper et al., 2007). As shown by bathymetric and seismic data obtained during several site surveys, drilling to 510 mbsf would penetrate through volcanic and biogenic sediment with intercalated large chaotic units (interpreted as debris avalanche Deposits 1 and 2). Of particular interest are the contacts between the different units, not only to distinguish between the different deposits but also to better understand mass transport dynamics, especially in the basal part of the flow. This study will provide fundamental constraints on friction parameters needed for realistic avalanche propagation models. Sediment above the deposit will be dated using δ¹⁸O chronostratigraphy to better constrain the age of this event. As shown on the seismic profiles, a thick and well-bedded sedimentary layer (~70 m) overlies Deposit 2 with an abnormal thickness toward the northeast. We will test the hypothesis that, following a flank collapse, the on-land drainage system is drastically modified, resulting in increased erosion and, therefore, increased sedimentation rates in the Grenada Basin.

Scientific results

Lithostratigraphy

Sediment retrieved at Site U1400 is divided into seven lithostratigraphic units (Units A–G) (Figs. F19, F20). Generally, this site is dominated by a combination of hemipelagic mud with interbedded tephra, volcaniclastic turbidites, and deformed sediment. Units A–G consist of varying proportions of these different lithologies. Unit A (0–27 mbsf in Hole U1400A and 0–2.94 mbsf in Hole U1400B mbsf) consists of dark gray massive volcanic sand, followed by hemipelagic mud and alternating layers of hemipelagic mud, tephra, and turbidite layers. Pumice is present in variable amounts (5% to >60%) throughout the entire unit. Unit B (27 to >51 mbsf in Hole U1400A, 2.94–25.5 mbsf in Hole U1400B, and 15–22 mbsf in Hole U1400C) is solely composed of volcaniclastic sand. Pumice and scoria clasts were found throughout the entire unit. Unit C (25.5–35 mbsf in Hole U1400B and 22–24.8 mbsf in Hole U1400C) is dominantly composed of gray-green hemipelagic mud with several tephra and two thin turbidite layers. Pumice is abundant in both the tephra layers and the turbidites, with some of the layers containing as much as 90% pumice. Unit D (35–58 mbsf in Hole U1400B and 24.8–59 mbsf in Hole U1400C) consists of gray and in some places highly mottled gray-green-brown hemipelagic mud with interbedded tephra layers (and a few turbidites in Hole U1400C). With the exception of the uppermost 3 m (inclination of layers = ~60°–70°), most of the sediment is weakly deformed (inclinations at ~20°) or contorted. Despite its relatively shallow present-day burial depth, the sediment is occasionally highly indurated. Most of the tephra layers contain pumice in various proportions. Unit E (58–212.5 mbsf in Hole U1400B and 59–190 mbsf in Hole U1400C) is composed of primarily hemipelagic mud with numerous interbedded tephra and turbiditic layers, ranging in thickness from a few tens of centimeters to several meters. Most of the tephra layers, as well as the turbidites, contain a significant amount of pumice (varying between 5% and 60%). Generally, the degree of sediment deformation in this unit is much higher (bedding inclination on average = 40° but ranging as high as 70°) than in other units. Unit F (190–390 mbsf in Hole U1400C) is composed of a succession of deformed (bedding and contact inclinations as high as 80°) and lithified hemipelagic sediment. The unit locally contains many tephra layers. A few muddy-sand debrite intervals, frequently rich in pumice clasts, are observed at different depths within the unit. Unit G (390 to a total depth of 436 mbsf) consists mainly of hemipelagic mud and partly lithified mudstone lacking any signs of sediment deformation. The top of this unit therefore marks the lower boundary of the deformed sediment.

Seventy-eight samples were taken to determine the mineralogical composition (XRD) and carbonate content of the cored sediment. In general, the mineralogy is very similar to the mineralogy obtained at Sites U1398 and U1399. However, subtle variations in the relative proportions of volcanic minerals are present, with quartz and Fe-Ti oxides being more abundant than those seen in the deeper sites. Clay minerals (typically smectite, kaolinite, and glauconite) were identified in virtually every sample and are present in high abundance in some samples. As is typical for sediment cores taken near volcanic islands, carbonate concentrations are highly variable and are lower in intervals with higher proportions of volcanic material. Maximum carbonate concentrations are ~35 wt%, also reflecting the greater proportion of terrestrial clay minerals and the absence of significant aragonite preservation. An unusual aspect of the organic carbon data is a general increase in concentrations with depth. Concentrations in the upper 250 mbsf are generally low (mostly <0.5 wt%) compared to previous sites, whereas approximately half the samples from this depth contain higher organic carbon concentrations, with some samples reaching 0.8 wt%.

Paleontology and biostratigraphy

Core catcher samples collected at Site U1400 for shipboard biostratigraphic studies contain calcareous nannofossils and planktonic and benthic foraminifers of varying abundances. Calcareous nannofossil and planktonic foraminiferal datums both resolve late Pleistocene ages for the majority of samples. However, at the base of each hole, species indicative of the Pliocene are present. Reworking is evident throughout the material cored at this site. The calcareous nannofossil species observed within the late Pleistocene material are mainly Emiliania huxleyi, Gephyrocapsa parallela, Gephyrocapsa oceanica, Ceratolithus cristatus, Ceratolithus telesmus, and Ceratolithus simplex. Assemblages observed at the base of the site characteristic for the late Pliocene are Discoaster brouweri, Discoaster surculus, Calcidiscus macintyrei, and Discoaster asymmetricus. These samples are assigned to Subzone CN12d. Globigerinoides ruber (white and pink), Globigerinoides sacculifer, and Neogloboquadrina dutertrei (dextral) dominate the assemblage of the planktonic foraminifers. Other abundant species include Pulleniatina obliquiloculata and Sphaeroidinellopsis dehiscens. In all holes, the population changes toward the base to reflect a likely Pliocene assemblage. This change is most obvious in Hole U1400C: in Sample 340-U1400C-36X-CC, P. obliquiloculata is reduced in number; it is absent in Sample 38X-CC, and Globorotalia miocenica and Globorotalia exilis become more abundant. All of these changes reflect a late Pliocene rather than an early Pleistocene foraminiferal assemblage. All species present are indicative of warm subtropical waters. Several datum species were found in all three holes. The most frequently encountered datum species was Globigerinella calida (B 0.22 Ma). At the bases of Hole U1400A (Sample 340-U1400A-7H-CC), Hole U1400B (Sample 340-U1400B-28H-CC), and Hole U1400C (Samples 340-U1400C-33X-CC through 49X-CC), Globigerinella miocenica (T 2.39 Ma) becomes quite abundant and most likely reflects the true age of the sediment. Other late Pliocene markers present include Globigerinoides extremus (T 1.99 Ma) and G. exilis (T 2.10 Ma), further corroborating the PL5 zonation. Early Pliocene datum species Globorotalia cibaoensis (T 4.60 Ma) was also found in low numbers throughout the late Pliocene sediment in Hole U1400C. Benthic foraminifers are not present in enough numbers to provide a reliable paleodepth estimate.

Paleomagnetism

Interpretation of the behavior of the geomagnetic field during the deposition of the cored sediment to derive a magnetostratigraphy that is solely based on the data is restricted to sediment deeper than ~385 mbsf because of substantial deformation of sediment in the overlying chaotic unit. Based solely on inclination data and because of XCB recovery and rifling of the declination data, negative inclination values tentatively suggest reversed polarity and ages older than 780 k.y. This calculation agrees with biostratigraphic ages for the site.

Physical properties

Generally, physical properties data obtained from the cored material show consistent changes depending on the lithology recovered (Figs. F19, F20). Magnetic susceptibility data show high values in volcaniclastic material and relatively low values (mostly <400 × 10^–5 SI) in hemipelagic sediment. P-wave velocity increases with depth. Above 80 mbsf, P-wave velocities are consistent with expected velocities for hemipelagic sediment undergoing normal compaction. Below 80 mbsf, P-wave velocity increases at a lower rate. The highest P-wave velocities are measured in the volcaniclastic sediment (typically ~1750 m/s) and the lowest in the hemipelagic sediment. Discrete measurements of P-wave velocity also indicate a downhole velocity increase in the hemipelagic mud. Again, the volcaniclastic material shows much higher velocities (1700–1840 m/s) than the hemipelagic mud (1650–1750 m/s). Porosity in the hemipelagic samples ranges between 51.5% and 73%, showing a weak decrease with increasing depth. Porosity in the volcaniclastic sand ranges between 36% and 51%. Observed bulk density in the hemipelagic sediment ranges between 1.5 and 1.82 g/cm³, displaying a very weak positive correlation with depth. Sandy samples have bulk densities as high as 2.18 g/cm³, quite distinct from the density of the hemipelagic samples. Grain density in the hemipelagic sediment varies between 2.53 and 2.77 g/cm³. Grain density in the volcaniclastic material varies between 2.74 and 2.87 g/cm³. Shear strength measurements showed a significant variability about a trend of shear stress increasing with depth. Sediment expansion observed during core cutting on the catwalk (Holes U1400B and U1400C) suggests that decompression reduces the undrained shear strength (S_u) of the sediment substantially after retrieval. Downhole temperature was measured using the APCT-3 at 48, 76, and 103 mbsf in Hole U1400C. The temperature gradient is 52.9° ± 1.6°C/km. Using the measured thermal conductivity of 1.050 W/(m·K), with standard on the mean of 0.006 W/(m·K), the implied conductive heat flow is 56 ± 4 mW/m². Bathymetry at this site decreases the near surface heat flow by 2%, and sedimentation lowers the near surface heat flow by as much as 4% (Manga et al., 2012). There is no evidence for fluid flow affecting temperature.

Geochemistry

Samples for headspace analyses were taken from 49 cores throughout all three holes at this site. In contrast to the two previous sites in the basin, not a single sample had a methane concentration >4.1 ppm, and the vast majority had concentrations of <3 ppm. No higher hydrocarbons were detected in any of the samples.

The pore water profiles can be, with the exception of the deepest sample from 427 mbsf, readily interpreted in terms of a classic diagenetic profile driven by the oxidation of organic carbon. Calcium and Mg are generally close to seawater value with some slight depletions, but Ca concentrations increase and Mg concentrations decrease with depth near the bottom of the sampled interval. The Cl data show a steady increase in concentration from the modern seawater value at the surface (560 mM) to 570 mM at 120 mbsf, likely reflecting progressive hydration of volcanic material as it is altered to clay minerals. It is interesting to note that the chemical composition of the deepest sample deviates from this interpretation; in particular, it has a much lower ΣS concentration than the rest of the samples. This sample comes from much older sediment (~2 m.y. old) that appears to be separated from the younger overlying sediment by a hiatus of at least 1 m.y. The two deepest samples also contain the highest organic carbon concentrations. Thus, the pore water geochemistry of the deepest sample seems to reflect a diagenetic environment distinct from that observed in the overlying sediment. This distinction either reflects changes in environmental conditions at this site over time or transport of the upper sediment to this area from a site of lower organic carbon deposition.

Site U1401

Background and objectives

IODP Site U1401 (proposed Site CARI-12A; 14°39.10′N, 61°25.08′W; 2590 mbsl) is west of Martinique (Fig. F11). Site U1401 was dedicated to the characterization of debris avalanche deposits and study of their emplacement processes. The Montagne Pelée Volcano has experienced at least three major flank-collapse events, which systematically destroyed the western flank of the volcano. Previous studies revealed the presence of a debris avalanche deposit with hummocky morphology associated with the 9000-year-old flank collapse (Le Friant et al., 2003; Boudon et al., 2007). Seismic site survey data indicated that Site U1401 could penetrate volcanic and biogenic sediment with intercalated large chaotic units (interpreted as debris avalanche deposits). We expected to drill through mass-wasting Deposit 3 and mass-wasting Deposit 2 from the Montagne Pelée Volcano with the aim of distinguishing the two deposits and also identifying erosive levels or frictional interactions between them. In addition, we expected to recover sediment from the top of the debris avalanche deposit which would allow better age constraint of the event. The data obtained from the sampled sediment will provide valuable insights into the chronology (one or several pulses), the mobility of debris avalanches, and the processes of possible syntransport flow transformation.

Scientific results

Lithostratigraphy

Sediment cored at Site U1401 was divided into three lithostratigraphic units (Units A–C) consisting of a combination of hemipelagic mud with interbedded tephra and/or volcaniclastic turbidites (Fig. F21). Unit A (0–8.4 mbsf in Hole U1401A, 0–7.6 mbsf in Hole U1401B, 0–5.7 mbsf in Hole U1401C, and 0–3.7 mbsf in Hole U1401D) is composed of a thick ungraded to weakly graded volcanic sand layer locally containing some light-colored lava/pumice granules. This sequence is followed by hemipelagic mud with numerous interbedded, poorly sorted, sometimes laminated volcanic sand layers. Most of these layers can be interpreted as tephra layers. However, the thicker layers show planar lamination and poor sorting, suggesting their emplacement was by density flows rather than fallout. In a few places, the sandy tephra layers are separated by fine brown mud, which is most likely volcanic in origin. Unit B (8.4–14.4 mbsf in Hole U1401A, 7.6–12.9 mbsf in Hole U1401B, 5.7–10.3 mbsf in Hole U1401C, and 3.7–9.25 mbsf in Hole U1401D) is composed of a series of coarse to very coarse volcaniclastic turbidites. These turbidites are as thick as 2 m and generally normally graded with a basal part rich in gravels and a top part composed of fine to medium sand. At least three or four distinct turbidites are observed. They contain pumices and scoriae in variable proportions, with vesiculated, massive, and oxidized lavas and crystals. The basal part is rich in granules and clasts of gray to reddish gray dense lavas; some of them reach 7 cm in size. The clasts comprise mainly two-pyroxene andesites or dacites. Interbedded hemipelagic mud in this unit was only observed in Holes U1401A and U1401D. Unit C (14.4–81.5 mbsf in Hole U1401A) is characterized by abundant mafic, vesicular andesite clasts as long as 7 cm, as well as subsidiary amounts of clasts of two-pyroxene andesite.

Paleontology and biostratigraphy

Core catcher samples from Site U1401 contain calcareous nannofossils and planktonic and benthic foraminifers in generally low abundance and were often found to be barren. Because of the coarse nature of the material collected, very few core catcher samples were adequate for biostratigraphic analysis. However, nannofossil and planktonic foraminiferal content were sufficient to resolve an age of late Pleistocene for this site. In Hole U1401A, Emiliania huxleyi and Gephyrocapsa sp. were observed, dating the material to younger than 0.08 Ma (Zone CN15, E. huxleyi acme zone). One sample (340-U1401D-1H-CC) contained abundant planktonic foraminifers, including Globigerinoides ruber (pink and white) and Globigerinoides sacculifer. One datum species, Globigerinella calida (B 0.22 Ma) was found in that sample, placing this sediment also within the late Pleistocene. No benthic foraminifers were found at this site.

Paleomagnetism

Interpretation of the behavior of the geomagnetic field during deposition of the cored sediment to derive a magnetostratigraphy is solely based on the generally discontinuous (restricted to the zone above 10 mbsf in all cores) record of hemipelagic sediment cored at this site. Expected inclination for the site is ±27.6°, assuming a GAD model. Inclination data all show positive values and normal GAD-like inclination. Declination shows some scatter, but coupled with the positive inclination data it suggests all sediment was deposited under normal polarity conditions. Using the GPTS of Cande and Kent (1995), this sediment was deposited in the Brunhes Chron and is younger than 780 ka. This agrees with the ages obtained from the biostratigraphic studies.

Physical properties

Physical properties data obtained from the cored material generally show differences based on the lithology retrieved (Fig. F21). In all three holes, peaks in magnetic susceptibility correspond to volcaniclastic beds (2000 × 10^–5 to 5000 × 10^–5 SI), whereas low magnetic susceptibility values (<2000 × 10^–5 SI) correspond to hemipelagic mud. In the uppermost 6 mbsf at Hole U1401A, bulk density progressively increases from 1.4 to 2.0 g/cm³ with depth despite several mud layers interlaced with volcaniclastic sand at these depths. We do not observe this trend in the other three holes at this site. Similar to the behavior of NGR observed at the other sites, NGR is strongly correlated with the mud content in the beds, with more mud resulting in higher NGR counts. The mud layer at ~10.3 mbsf in Hole U1401B has the highest value of 21 cps. The two major lithologies are also clearly identified in P-wave velocity patterns, showing low values in the hemipelagic mud (1500–1650 m/s) and higher values in the volcaniclastic material (1650–1800 m/s; maximum of 1860 m/s). Measurements of P-wave velocity obtained from discrete samples also resemble this pattern; hemipelagic mud has velocities of 1530–1660 m/s, whereas volcaniclastic sand has velocities of 1720–1920 m/s. Density and porosity values obtained from hemipelagic sediment are typical for shallow, buried marine sediment. Porosities are between 50% and 60%, and grain densities are ~2.75 g/cm³. Although measurements are limited, shear strength generally increases with depth from 3–5 kPa in the upper few meters to 20 kPa at 15 mbsf.

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