Expedition 350 methods - University of Tasmania

Tamura Y Busby CJ Blum P and the Expedition 350 Scientists 2015Proceedings of the International Ocean Discovery Program Volume 350publicationsiodporg

doi1014379iodpproc3501022015

Expedition 350 methods 1

Y Tamura CJ Busby P Blum G Guegraverin GDM Andrews AK Barker JLR Berger EM Bongiolo M Bordiga SM DeBari JB Gill C Hamelin J Jia EH John A-S Jonas M Jutzeler MAC Kars ZA Kita K Konrad SH Mahoney M Martini T Miyazaki RJ Musgrave DB Nascimento ARL Nichols JM Ribeiro T Sato JC Schindlbeck AK Schmitt SM Straub MJ Vautravers and Y Yang2

Keywords International Ocean Discovery Program IODP JOIDES Resolution Expedition 350 Site U1436 Site U1437 Izu-Bonin-Mariana IBM prehnite rear arc seamount Manji tuffaceous mud volcaniclastic hyaloclastite zircon Neogene ash pumice tuff lapilli Quaternary breccia peperite rhyolite intrusive subduction glass continental crust fore arc density current turbidite fall deposit tephra greigite volcano-bounded basin VBB hemipelagic mud caldera andesite pXRF ICP-AES bioturbation hydrothermal alteration smectite hornblende sulfide reduction fiamme diagenesis Aogashima Kuroshio explosive volcanism submarine volcanism

1 Tamura Y Busby CJ Blum P Guegraverin G Andrews GDM Barker AK Berger JLR Bongiolo EM Bordiga M DeBari SM Gill JB Hamelin C Jia J John EH Jonas A-S Jut-zeler M Kars MAC Kita ZA Konrad K Mahoney SH Martini M Miyazaki T Musgrave RJ Nascimento DB Nichols ARL Ribeiro JM Sato T Schindlbeck JC Schmitt AK Straub SM Vautravers MJ and Yang Y 2015 Expedition 350 methods In Tamura Y Busby CJ Blum P and the Expedition 350 Scientists Proceedings of the International Ocean Discovery Program Expedition 350 Izu-Bonin-Mariana Rear Arc College Station TX (International Ocean Discovery Program) httpdxdoiorg1014379iodpproc3501022015

2 Expedition 350 Scientistsrsquo addressesMS 350-102 Published 30 May 2015

Contents

1 Introduction4 Lithostratigraphy

15 Geochemistry20 Physical properties23 Paleomagnetism27 Biostratigraphy32 Age model35 Downhole measurements39 References

IntroductionThis chapter of the International Ocean Discovery Program

(IODP) Expedition 350 Proceedings volume documents the proce-dures and tools employed in the various shipboard laboratories of the RV JOIDES Resolution during Expedition 350 This informa-tion applies only to shipboard work described in the Expedition Re-ports section of this volume Methods for shore-based analyses of Expedition 350 samples and data will be described in the individual scientific contributions to be published in the open literature or in the Expedition Research Results section of this volume

This section describes procedures and equipment used for drill-ing coring and hole completion core handling computation of depth for samples and measurements and sequence of shipboard analyses Subsequent sections describe specific laboratory proce-dures and instruments in more details

OperationsSite locations

GPS coordinates from precruise site surveys were used to posi-tion the vessel at all Expedition 350 sites A SyQuest Bathy 2010 CHIRP subbottom profiler was used to monitor the seafloor depth on the approach to each site to reconfirm the depth profiles from precruise surveys Once the vessel was positioned at a site the thrusters were lowered and a positioning beacon was dropped to the seafloor The dynamic positioning control of the vessel used navigational input from the GPS and triangulation to the seafloor

beacon weighted by the estimated positional accuracy The final hole position was the mean position calculated from the GPS data collected over a significant portion of the time the hole was occu-pied

Coring and drilling operationsThe coring strategy for Expedition 350 consisted primarily of

obtaining as deep a penetration as possible at one site The first hole would consist of a jet-in test to establish that a 16 inch casing de-ployed with the reentry cone could be washed in to ~25 meters be-low seafloor (mbsf ) The second hole would be cored with the full-length advanced piston corer (APC) and the half-length APC (HLAPC) systems to refusal and deepened with the extended core barrel (XCB) system to ~400ndash600 mbsf A third hole would be cored with the rotary core barrel (RCB) system from the maximum depth of the APCXCB hole and penetrate as deep as possible The fourth hole would be drilled without coring to the maximum depth of the existing RCB hole then be cased and then extended as deep as time permitted A secondary component was to drill a 150 m APC hole at the beginning of the cruise to provide geotechnical information for a potential ultradeep riser hole to be drilled with the DV Chikyu

The APC and HLAPC cut soft-sediment cores with minimal coring disturbance relative to other IODP coring systems and are suitable for the upper portion of each hole After the APC core bar-rel is lowered through the drill pipe and lands near the bit the drill pipe is pressured up until one or two shear pins that hold the inner barrel attached to the outer barrel fail The inner barrel then ad-

Y Tamura et al Expedition 350 methods

vances into the formation at high speed and cuts the core with a di-ameter of 66 mm (26 inches) The driller can detect a successfulcut or ldquofull strokerdquo from the pressure gauge on the rig floor

The depth limit of the APC often referred to as APC refusal isindicated in two ways (1) the piston fails to achieve a completestroke (as determined from the pump pressure reading) because theformation is too hard or (2) excessive force (gt60000 lb ~267 kN) isrequired to pull the core barrel out of the formation When a fullstroke could not be achieved additional attempts were typicallymade The assumption is made that the barrel penetrated the for-mation by the length of core recovered (nominal recovery of~100) and the bit was advanced by that length before cutting thenext core When a full or partial stroke was achieved but excessiveforce could not retrieve the barrel the core barrel was sometimesldquodrilled overrdquo meaning after the inner core barrel was successfullyshot into the formation the drill bit was advanced to total depth tofree the APC barrel

Nonmagnetic core barrels were used during all APC deploy-ments except during the return to Site U1436 at the end of the ex-pedition when no paleomagnetic measurements were neededMost APC cores recovered during Expedition 350 were oriented us-ing the FlexIT tool (see Paleomagnetism) Formation temperaturemeasurements were made to obtain temperature gradients and heatflow estimates (see Downhole measurements)

The XCB is a rotary system with a small cutting shoe that ex-tends below the large rotary APCXCB bit The smaller bit can cut asemi-indurated core with less torque and fluid circulation than themain bit optimizing recovery The XCB cutting shoe (bit) extends~305 cm ahead of the main bit in soft sediment but retracts into themain bit when hard formations are encountered It cuts a core withnominal diameter of 587 cm (2312 inches) slightly less than the 66cm diameter of the APC cores

The RCB is the most conventional rotary coring system and issuitable for lithified rock material It cuts a core with nominal diam-eter of 587 cm just as the XCB system does RCB coring can bedone with or without the core liners used routinely with theAPCXCB soft sediment systems We chose to core without theliner in the deeper parts of Hole U1437E because core piecesseemed to get caught at the edge of the liner leading to jammingand reduced recovery

The bottom-hole assembly (BHA) is the lowermost part of thedrill string A typical APCXCB BHA consists of a drill bit (outerdiameter = 11 inches) a bit sub a seal bore drill collar a landingsaver sub a modified top sub a modified head sub a nonmagneticdrill collar (for APCXCB) a number of 8 inch (~2032 cm) drill col-lars a tapered drill collar 6 joints (two stands) of 5frac12 inch (~1397cm) drill pipe and 1 crossover sub A lockable flapper valve wasused to collect downhole logs without dropping the bit whenAPCXCB coring

A typical RCB BHA consists of a drill bit a bit sub an outer corebarrel a top sub a head sub 8 joints of 8frac14 inch drill collars a ta-pered drill collar 2 joints of standard 5frac12 inch drill pipe and a cross-over sub to the regular 5 inch drill pipe

The typical casing installation consists of 20 inch casing about25 m long attached to a reentry cone with a casing hanger that re-ceives a 16 inch casing string a few hundred meters long and finallya 10frac34 inch string of several hundred meters length Installation ofthe casing in Hole U1437E which represents a record length for theJOIDES Resolution (10856 m) is described in Operations in theSite U1437 chapter (Tamura et al 2015)

Drilling disturbanceCores may be significantly disturbed as a result of the drilling

process and contain extraneous material as a result of the coringand core handling process In formations with loose granular layers(sand ash shell hash ice-rafted debris etc) granular material fromintervals higher in the hole may settle and accumulate in the bottomof the hole as a result of drilling circulation and be sampled with thenext core The uppermost 10ndash50 cm of each core must therefore beexamined critically during description for potential ldquofall-inrdquo Com-mon coring-induced deformation includes the concave-downwardappearance of originally horizontal bedding Piston action may re-sult in fluidization (flow-in) at the bottom of or even within APCcores Retrieval of unconsolidated (APC) cores from depth to thesurface typically results to some degree in elastic rebound and gasthat is in solution at depth may become free and drive core seg-ments within the liner apart When gas content is high pressuremust be relieved for safety reasons before the cores are cut into seg-ments This is accomplished by drilling holes into the liner whichforces some sediment as well as gas out of the liner XCB coring typ-ically affects torquing of the indurated core resulting in fractureddisc-shaped pieces packed with sheared and remolded core mate-rial mixed with drill slurry resembling resembled soft cream be-tween brittle ldquobiscuitsrdquo

Drilling disturbances are described in the Lithostratigraphy sec-tions in each site chapter and are graphically indicated on thegraphic core summary reports also referred to as visual core de-scriptions (VCDs) in Core descriptions

Core handling and analysisAll APC and XCB cores and some of the RCB cores recovered

during Expedition 350 were extracted from the core barrel in plasticliners These liners were carried from the rig floor to the core pro-cessing area on the catwalk outside the Core Laboratory and cutinto ~15 m sections The exact section length was noted and laterentered into the database as ldquocreated lengthrdquo using the Sample Mas-ter application This number was used to calculate recovery Thecurated length was set equal to the created length and very rarelyhad to be modified Depth in hole calculations are based on the cu-rated length

When the core liners seemed to cause jams preventing pieces toenter the barrel liners were not used Instead the recovered corewas slid and shaken out of the barrel and carefully arrange in theorder retrieved in a prepared half-liner The core pieces were thenfilled into a full liner for the purpose of splitting We did not per-form any ldquohard rock curationrdquo whereby pieces are separated with di-viders and logged separately

Headspace samples were taken from selected section ends (typi-cally 1 per core) using a syringe for immediate hydrocarbon analysisas part of the shipboard safety and pollution prevention programSimilarly whole-round samples for interstitial water analysis andmicrobiology samples were taken immediately after the core wassectioned Core catcher samples were taken for biostratigraphicanalysis When catwalk sampling was complete liner caps (blue =top colorless = bottom) were glued with acetone onto liner sec-tions and the sections were placed in core racks in the laboratoryfor analysis

After completion of whole-round section analyses (see below)the sections were split lengthwise from bottom to top into workingand archive halves The softer cores were split with a wire and

IODP Proceedings 2 Volume 350


harder cores were split with a diamond saw Investigators shouldnote that older material may have been transported upward on thesplit face of each section during splitting

The numbering of sites holes cores and samples followed stan-dard IODP procedure A full curatorial sample identifier consists ofthe following information expedition site hole core number coretype section number section half and offset in centimeters mea-sured from the top of the core section For example a sample iden-tification of ldquo350-U1436A-1H-2W 10ndash12 cmrdquo represents a sampletaken from the interval between 10 and 12 cm below the top of theworking half of Section 2 of Core 1 (ldquoHrdquo designates that this corewas taken with the APC system) of Hole U1436A during Expedition350 The ldquoUrdquo preceding the site number indicates that the hole wasdrilled by the United States Implementing Organization (USIO)platform the JOIDES Resolution

Sample depth calculationsSample depth calculations are based on the methods described

in IODP Depth Scales Terminology v2 at wwwiodporgprogram-policiesproceduresguidelines Depths of samples and measure-ments were calculated at the applicable depth scale as summarizedbelow The definition of these depth scale types and the distinctionin nomenclature should keep the user aware that a nominal depthvalue at two different depth scale types usually does not refer to ex-actly the same stratigraphic interval in a hole

Depths of cored intervals were measured from the drill floorbased on the length of drill pipe deployed beneath the rig floor andreferred to as drilling depth below rig floor (DRF) with a commonlyused custom unit designation of meters below rig floor (mbrf ) Thedepth of the cored interval was referenced to the seafloor by sub-tracting the seafloor depth from the DRF depth of the interval Theseafloor referenced depth of the cored interval is referred to as thedrilling depth below seafloor (DSF) with a commonly used customunit designation of meters below seafloor (mbsf) In most cases theseafloor depth was the length of pipe deployed minus the length ofthe mudline core recovered In some cases the seafloor depth wasadopted from a previous hole drilled at the site

Depths of samples and measurements in each core are com-puted based on a set of rules that result in a depth scale type re-ferred to as the core depth below seafloor Method A (CSF-A) Thetwo most fundamental rules are that (1) the top depth of a recoveredcore corresponds to the top depth of its cored interval (top DSF =top CSF-A) even if the core includes fall-in material at the top (seeDrilling disturbance) and (2) the recovered material is a contigu-ous stratigraphic representation even if core segments are sepa-rated by voids when recovered and if the core is shorter than thecored interval When voids were present in the core on the catwalkthey were closed by pushing core segments together whenever pos-sible When a core had incomplete recovery (ie the true position ofthe core within the cored interval was unknown) the top of the re-covered interval was assigned to the top of the cored interval Thelength of missing core should be considered a sample depth uncer-tainty when analyzing data associated with the core materialDepths of subsamples and associated measurements at the CSF-Ascale were calculated by adding the offset of the subsample or mea-surement from the top of its section and the lengths of all highersections in the core to the top depth of the cored interval (top DSF= top CSF-A)

Per IODP policy established after the introduction of the IODPDepth Scales Terminology v2 sample and measurement depths atthe CSF-A depth scale type are commonly referred to with the cus-

tom unit mbsf just as depths at the DSF scale type The readershould be aware that the use of mbsf for different depth scale typesis inconsistent with the more rigorous definition of depth types andmay be misleading in specific cases because different ldquombsf depthsrdquomay be assigned to the same stratigraphic interval One example isdescribed below

A soft to semisoft sediment core from less than a few hundredmeters below seafloor expands upon recovery (typically a few per-cent to as much as 15) so the length of the recovered core exceedsthat of the cored interval Therefore a stratigraphic interval maynot have the same nominal depth at the DSF and CSF-A scales inthe same hole When core recovery (the ratio of recovered core tocored interval times 100) is gt100 the CSF-A depth of a sampletaken from the bottom of a core will be deeper than that of a samplefrom the top of the subsequent core (ie the data associated withthe two core intervals overlap at the CSF-A scale) The core depthbelow seafloor Method B (CSF-B) depth scale is a solution to theoverlap problem This method scales the recovered core length backinto the interval cored from gt100 to exactly 100 recovery Ifcores had lt100 recovery to begin with they were not scaledWhen downloading data using the IODP-USIO Laboratory Infor-mation Management System (LIMS) Reports pages atwebiodptamueduUWQ depths for samples and measurementsare by default presented at both CSF-A and CSF-B scales TheCSF‑B depth scale is primarily useful for data analysis and presenta-tions in single-hole situations

Another major depth scale type is the core composite depth be-low seafloor (CCSF) scale typically constructed from multiple holesfor each site whenever feasible to mitigate the CSF-A core overlapproblem as well as the coring gap problem and to create as continu-ous a stratigraphic record as possible This depth scale type was notused during Expedition 350 and is therefore not further describedhere

Shipboard core analysisAfter letting the cores thermally equilibrate for at least 1 h

whole-round core sections were run through the Whole-RoundMultisensor Logger (WRMSL) which measures P-wave velocitydensity and magnetic susceptibility and the Natural Gamma Radia-tion Logger (NGRL) Thermal conductivity measurements werealso taken before the cores were split lengthwise into working andarchive halves The working half of each core was sampled for ship-board analysis routinely for paleomagnetism and physical proper-ties and more irregularly for thin sections geochemistry andbiostratigraphy The archive half of each core was scanned on theSection Half Imaging Logger (SHIL) and measured for color reflec-tance and magnetic susceptibility on the Section Half MultisensorLogger (SHMSL) The archive halves were described macroscopi-cally as well as microscopically in smear slides and the workinghalves were sampled for thin section microscopic examination Fi-nally the archive halves were run through the cryogenic magnetom-eter Both halves of the core were then put into labeled plastic tubesthat were sealed and transferred to cold storage space aboard theship

Samples for postcruise analysis were taken for individual inves-tigators from the working halves of cores based on requests ap-proved by the Sample Allocation Committee (SAC) Up to 17 coreswere laid out in 13 sampling parties lasting 2ndash3 days each fromplanning to execution Scientists viewed the cores flagged samplinglocations and submitted detailed lists of requested samples TheSAC reviewed the flagged samples and resolved rare conflicts as



needed Shipboard staff cut registered and packed the samples Atotal of 6372 samples were taken for shore-based analyses in addi-tion to 3211 samples taken for shipboard analysis

All core sections remained on the ship until the end of Expedi-tion 351 because of ongoing construction at the Kochi Core Center(KCC) At the end of Expedition 351 all core sections and thin sec-tions were trucked to the KCC for permanent storage

LithostratigraphyLithologic description

The lithologic classification of sedimentary volcaniclastic andigneous rocks recovered during Expedition 350 uses a new scheme

for describing volcaniclastic and nonvolcaniclastic sediment (FigureF1) but uses generally established (International Union of Geologi-cal Sciences [IUGS]) schemes for igneous rocks This new schemewas devised to improve description of volcaniclastic sediment andthe mixtures with nonvolcanic (siliciclastic and chemical and bio-genic) sediment while maintaining the usefulness of prior schemesfor describing nonvolcanic sediment The new scheme follows therecommendations of a dedicated core description workshop held inJanuary 2014 in College Station (TX USA) prior to the cruise andattended by participants of IODP Expeditions 349 350 351 and352 and was tested and finalized during Expedition 350 The newscheme was devised for use in a spreadsheet-based descriptive in-formation capture program designed by IODP (DESClogik) and the

Figure F1 New sedimentary and volcaniclastic lithology naming conventions based on relative abundances of grain and clast types Principal lithology namesare compulsory for all intervals Prefixes are optional except for tuffaceous lithologies Suffixes are optional and can be combined with any combination ofprefixprincipal name First-order division is based on abundance of volcanic-derived grains and clasts gt25 volcanic grains is of either ldquovolcanicrdquo (gt75volcanic grains named from grain size classification of Fisher and Schmincke 1984 [orange]) or ldquotuffaceousrdquo (25ndash75 volcanic grains) Tuffaceous lithologiesif dominant nonvolcanic grain component is siliciclastic the grain size classification of Wentworth (1922 green) was used if not siliciclastic it is named by thedominant type of carbonate chemical or biogenic grain (blue) Lithologies with 0ndash25 volcanic grains are classified as ldquononvolcanicrdquo and treated similarly totuffaceous lithologies when nonvolcanic siliciclastic sediment dominates the grain size classification of Wentworth (1922 green) is used when the combinedcarbonate other chemical and biogeneic sediment dominate the principal lithology is taken from the dominant component type (blue) Closely intercalatedintervals can be grouped as domains to avoid repetitive entry at the small-scale level

Matrix-supported monomictic mafic ash with ashMatrix-supported polymictic mafic tuff with tuffMatrix-supported monomictic evolved lapilli-ash with lapilli-ashMatrix-supported polymictic evolved lapilli-tuff with lapilli-tuffMatrix-supported monomictic lapilli with lapilliMatrix-supported polymictic lapillistone with lapillistoneClast-supported monomictic mafic ash-breccia with ash-brecciaClast-supported polymictic mafic tuff-breccia with tuff-brecciaClast-supported monomictic evolved unconsolidated volcanic conglomerate with volcanic conglomerateClast-supported polymictic evolved consolidated volcanic conglomerate with volcanic breccia-conglomerateClast-supported monomictic unconsolidated volcanic breccia-conglomerate with volcanic brecciaClast-supported polymictic consolidated volcanic breccia-conglomerate with dense glass lapilliMafic unconsolidated volcanic breccia with accretionary lapilliEvolved consolidated volcanic breccia with pillow fragment lapilliBimodal with lithic lapilli

with crystalswith scoria lapilliwith pumice lapilli

clay with ash podclaystone with clay silt with claystone siltstone with silt fine sand with siltstone fine sandstone with sand medium to coarse sand with sandstone medium to coarse sandstone with conglomeratesand with breccia-conglomeratesandstone with brecciamud with fine sandmudstone with fine sandstoneunconsolidated conglomerate with medium to coarse sandconsolidated conglomerate with medium to coarse sandstoneunconsolidated breccia-conglomerate with mudconsolidated breccia-conglomerate with mudstoneunconsolidated breccia with microfossilsconsolidated breccia with foraminifer

with biosiliceous ooze with biosiliceous chalk with calcareous ooze

biosiliceous ooze with calcareous chalk biosiliceous chalk with diatom ooze calcareous ooze with diatomite calcareous chalk with radiolarian ooze diatom ooze with radiolarite diatomite with foraminiferal ooze radiolarian ooze with foraminiferal chalk radiolarite with chertforaminiferal ooze with plant fragmentsforaminiferal chalk with fecal pelletschert with shells

1st line most abundant facies - one of the above 1st line 2nd most abundant facies- one of the above

1st line Closely intercalated2nd line PREFIX most abundant facies 2nd line PRINCIPAL NAME most abundant facies

2nd line SUFFIX most abundant facies3rd line PREFIX 2nd most ab facies 3rd line PRINCIPAL NAME 2nd most ab facies3rd line SUFFIX 2nd most ab facies4th line PREFIX 3rd most ab facies 4th line PRINCIPAL NAME 3rd most ab facies

4th line SUFFIX 3rd most ab facies

Matrix-supported monomicticMatrix-supported polymicticClast-supported monomicticClast-supported polymictic

Prefix (optional unless tuffaceous) Principal name (required) Suffix (optional)Lithologic classes

gt25

v

olca

nic

grai

ns a

nd c

last

s

Tuffaceous clast-supported polymictic

lt25

v

olca

nic

grai

ns a

nd

clas

ts

nonv

olca

nic

ANY closely intercalated

Volcanic(gt75 volcanic

grains and clasts)

Tuffaceous(25-75

volcanic grainsand clasts)

Nonvolcanicsiliciclastic

(nonvolcanicsiliclastic gtcarbonate +chemical +biogenic)

Carbonatechemical and

biogenic(nonvolcanicsiliclastic ltcarbonate +chemical +biogenic)

Tuffaceous matrix-supported polymictic Tuffaceous


jim
Highlight


spreadsheet configurations were modified to use this scheme Alsoduring Expedition 350 the new scheme was applied to microscopicdescription of core samples and the DESClogik microscope spread-sheet configurations were modified to use this scheme

During Expedition 350 all sediment and rock types were de-scribed by a team of core describers with backgrounds principally inphysical volcanology volcaniclastic sedimentation and igneous pe-trology Macroscopic descriptions were made at dedicated tableswhere the split core sections were laid out Each core section wasdescribed in two steps (1) hand-written observations were re-corded onto 11 inch times 17 inch printouts of high-resolution SHILimages and (2) data were entered into the DESClogik software (seebelow) This method provides two description records of each coreone physical and one digital and minimizes data entry mistakes inDESClogik Smear slides and petrographic thin sections were inves-tigated with binocular and petrographic microscopes (transmittedand reflected light) and described in DESClogik Because of the de-lay (about 24 h) required in producing petrographic thin sectionsonly smear slides could be used to contribute to macroscopic de-scriptions at the time the cores were described Thin section de-scriptions were used later to refine the initial macroscopicobservations

IODP use of DESClogikData for the macroscopic and microscopic descriptions of

recovered cores were entered into the LIMS database using theIODP data-entry software DESClogik DESClogik is a coredescription software interface used to enter macroscopic andormicroscopic descriptions of cores Core description data are avail-able through the Descriptive Information LIMS Report(webiodptamueduDESCReport) A single row in DESClogikdefines one descriptive interval which is commonly (but not neces-sarily) one bed (Table T1)

Core disturbancesIODP coring induces various types of disturbances in recovered

cores Core disturbances are recorded in DESClogik Core distur-

bances are diverse (Jutzeler et al 2014) and some of them are onlyassociated with specific coring techniques

bull Core extension (APC) preferentially occurs in granular (nonco-hesive) sediment This disturbance is obvious where sediment does not entirely fill the core liner and soupy textures occur Stratification is commonly destroyed and bed thickness is artifi-cially increased

bull Sediment flowage disturbance (APC) is the result of material displacement along the margins of the core liner This results in horizontal superposition of the original stratigraphy enveloped in allochthonous material

bull Mid-core flow-in (APC) is injection of material within the origi-nal stratigraphy Developing from sediment flowage alloch-thonous sediment is intruded into the genuine stratigraphy cre-ating false beds This disturbance type is rare and is commonly associated with strong shearing and sediment flowage along the margin of the core liner

bull Basal flow-in (APC) is associated with partial strokes in sedi-ment and occurs where cohesive muddy beds are absent from the bottom of the core Basal flow-in results from the sucking-in of granular material from the surrounding sediment through the cutting shoe during retrieval of the core barrel It creates a false stratigraphy commonly composed of soupy polymictic den-sity-graded sediment that generally lacks horizontal laminations (indicating homogenization) Basal flow-in disturbances can af-fect more than half of the core

bull Fall-in (APC XCB and RCB) disturbances result from collapse of the unstable borehole or fall-back of waste cuttings that could not be evacuated to the seafloor during washing with drilling water Fall-in disturbances occur at the very top of the core (ie usually most prevalent in Section 1 and rarely continues into the lower core sections) and often follow a core that was a partial stroke Fall-in disturbances commonly consist of polymictic millimeter to centimeter clasts and can be clast or matrix sup-ported The length of a fall-in interval is typically on the order of 10ndash40 cm but can exceed 1 m A fall-in interval is recognized by being distinctly different from the other facies types in the lower

Table T1 Definition of lithostratigraphic and lithologic units descriptive intervals and domains Download table in csv format

JOIDES ResolutionTypical thickness

range (m)JOIDES Resolution data

logging spreadsheet context Traditional sediment drillingTraditional igneous

rock drillingComparable nondrilling

terminology

Lithostratigraphic unit 101sim103 One row per unit in lithostrat summary tab numbered I II IIa IIb III etc

Used as specified however often referred to as lithologic unit in the past

Typically not used when only igneous rocks are drilled

Not specified during field campaign Formal names need to be approved by stratigraphic commission

Lithologic unit 10ndash1sim101 One row per unit in lith_unit summary tab numbered 1 2 3 4 etc

Typically not used because descriptive intervals correspond to beds which are directly summarized in lithostratigraphic units Similar concept facies type however those are not contiguous

Often defined previously as lava flows etc and used in the sense of a descriptive interval Enumerated contiguously as Unit 1 2 3 etc As defined here units may correspond to one or more description intervals

Sedimentology group of beds

Descriptive interval 10ndash1sim101 Primary descriptive entity that can be readily differentiated during time available One row per interval in principal logging tab (lithology specific)

Typically corresponds to beds If beds are too thin a thicker interval of intercalated is created and 2minus3 domains describe the characteristics of the different types of thin beds

Typically corresponds to the lithologic unit As defined here a lithologic unit may correspond to one or more description intervals

Sedimentology thinnest bed to be measured individually within a preset interval (eg 02 m 1 m 5 m etc) which is determined based on time available

Domain Same as parent descriptive interval

Additional rows per interval in principal logging tab below the primary description interval row numbered 1 2 etc (with description interval numbered 0)

Describes types of beds in an intercalated sequence can be specified in detail as a group

Describes multiple lithologies in a thin section or textural domains in a macroscopic description

Feature description within descriptive interval as needed



part of the same core displaying chaotic or massive bedding and containing constituents encountered further up in the hole

bull Fractured rocks (XCB and RCB) occur over three fracturing in-tensities (slight moderate and severe) but do not show clast ro-tation (Figure F2)

bull Brecciated and randomly oriented fragmented rocks (XCB and RCB) occur where rock fracturing was followed by remobiliza-tion and reorientation of the fragments into a disordered pseudostratigraphy (Figure F2)

bull Biscuited disturbances (XCB and RCB) consist of intervals of mud and brecciated rock They are produced by fragmentation of the core in multiple disc-shaped pieces (biscuits) that rotate against each other at different rates inducing abrasion and com-minution Biscuiting commonly increases in intensity toward the base of a core (Figure F2) Interstitial mud is either the orig-inal lithology andor a product of the abrasion Comminuted rock produces mud-sized gouges that can lithify and become in-distinguishable from fine-grained beds (Piper 1975)

Sediments and sedimentary rocksRationale

Sediments and sedimentary rocks are classified using a rigor-ously nongenetic approach that integrates volcanic particles intothe sedimentary descriptive scheme typically used by IODP (FigureF1) This is necessary because volcanic particles are the most abun-dant particle type in arc settings like those drilled during the Izu-Bonin-Mariana (IBM) expeditions The methodology developed al-lows for the first time comprehensive description of volcanogenicand nonvolcanogenic sediment and sedimentary rock and inte-grates with descriptions of coherent volcanic and igneous rock (ielava and intrusions) and the coarse clastic material derived fromthem This classification allows expansion to bioclastic and nonvol-canogenic detrital realms

The purpose of the new classification scheme (Figure F1) is toinclude volcanic particles in the assessment of sediment and rockrecovered in cores be accessible to scientists with diverse researchbackgrounds and experiences allow relatively quick and smoothdata entry and display data seamlessly in graphical presentationsThe new classification scheme is based entirely on observations thatcan be made by any scientist at the macroscopic and microscopiclevel with no genetic inferences making the data more reproduc-ible from user to user

Classification and nomenclature of deposits with volcanogenicclasts has varied considerably throughout the last 50 y (Fisher 1961Fisher and Schmincke 1984 Cas and Wright 1987 McPhie et al1993 White and Houghton 2006) and no consensus has yet beenreached Moreover even the most basic descriptions and character-izations of mixed volcanogenic and nonvolcanogenic sediment arefraught with competing philosophies and imperfectly applied ter-minology Volcaniclastic classification schemes are all too oftenoverly based on inferred modes of genesis including inferred frag-mentation processes or inferred transport and depositional pro-cesses and environments However submarine-erupted anddeposited volcanic sediments are typically much more difficult tointerpret than their subaerial counterparts partly because of morecomplex density-settling patterns through water relative to air andthe ease with which very fine grained sediment is reworked by wa-ter Soft-sediment deformation bioturbation and low-temperaturealteration are also more significant in the marine realm relative tothe terrestrial realm

In our new classification scheme some common lithologic pa-rameters are broader (ie less narrowly or strictly applied) thanthose used in the published literature this has been done (1) to re-duce unnecessary detail that is in the realm of specialist sedimento-logy and physical volcanology and make the descriptive processmore accessible intuitive and comprehensible to nonspecialistsand (2) to make the descriptive process as linear and as ldquodatabasereadyrdquo as possible

Description workflowThe following workflow was used

1 Initial determination of intervals in a core section was con-ducted by a pair of core describers (typically a physical volcan-ologist and an igneous petrologist) Macroscopic analyses were performed on all intervals for a first-order assessment of their main characteristics particle sizes compositions and heteroge-neity as well as sedimentary structures and petrofabrics If an interval described in the macroscopic sediment data sheet had igneous clasts larger than 2 cm the clasts were described in de-tail on the extrusivehypabyssal data sheet (eg crystallinity mineralogy etc) because clasts of that size are large enough to be described macroscopically

2 Microscopic analyses were performed for each new facies using (i) discrete samples diluted in water (not curated) (ii) sediment glued into a smear slide or (iii) petrographic thin sections of sediment or sedimentary rock Consistency was regularly checked for reoccurring facies Thin sections and smear slides varied in quantity and proportion depending on the firmness of the material the repetitiveness of the facies and the time avail-

Figure F2 Visual interpretation of core disturbances in semilithified and lithi-fied rocks in 350-U1437B-43X-1A 50ndash128 cm (left) and 350-U1437D-12R-6A 34ndash112 cm (right)

Biscuits core disturbance

Incr

easi

ng

bisc

uitin

g in

tens

ity

Slig

htM

oder

ate

Sev

ere

Des

troy

ed

Slig

htM

oder

ate

Sev

ere

Incr

easi

ng fr

actu

re in

tens

ity

Fracture core disturbance



able during core description Microscopic observations allow detailed descriptions of smaller particles than is possible with macroscopic observation so if a thin section described in the microscopic sediment data sheet had igneous clasts larger than 2 mm (the cutoff between sandash and granuleslapilli see defi-nitions below) the clasts were described in detail on the igneous microscopic data sheet

3 The sediment or sedimentary rock was named (Figure F1)4 A single lithologic summary sentence was written for each core

UnitsSediment and sedimentary rock including volcaniclastic silici-

clastic and bioclastic are described at the level of (1) the descrip-tive interval (a single descriptive line in the DESClogik spreadsheet)and (2) the lithostratigraphic unit

Descriptive intervalsA descriptive interval (Table T1) is unique to a specific depth

interval and typically consists of a single lithofacies distinct fromthose immediately above and below (eg an ash interval interca-lated between mud intervals) Descriptive intervals are thereforetypically analogous to beds and thicknesses can be classified in thesame way (eg Ingram 1954) Because cores are individually de-scribed per core section a stratigraphically continuous bed may bedivided into two (or more) intervals if it is cut by a corecore sectionboundary

In the case of closely intercalated monotonous repetitive suc-cessions (eg alternating thin sand and mud beds) lithofacies maybe grouped within the descriptive interval This is done by using thelithology prefix ldquoclosely intercalatedrdquo followed by the principalname which represents the most abundant facies followed by suf-fixes for the subordinate facies in order of abundance (Figure F1)Using the domain classifier in the DESClogik software the closelyintercalated interval is identified as Domain 0 and the subordinateparts are identified as Domains 1 2 and 3 respectively and theirrelative abundances noted Each subordinate domain is describedbeneath the composite descriptive interval as if it were its own de-scriptive interval but each subordinate facies is described onlyonce allowing simplified data entry and graphical output This al-lows for each subordinate domain to be assigned its own prefixprincipal name and suffix (eg a closely intercalated tuff with mud-stone can be expanded to evolved tuff with lapilli [Domain 1 80]and tuffaceous mudstone with shell fragments [Domain 2 20])

Lithostratigraphic unitsLithostratigraphic units not to be confused with lithologic units

used with igneous rocks (see below) are meters to hundreds of me-

ters thick assemblages of multiple descriptive intervals containingsimilar facies (Table T1) They are numbered sequentially (Unit IUnit II etc) from top to bottom Lithostratigraphic units should beclearly distinguishable from each other by several characteristics(eg composition bed thickness grain size class and internal ho-mogeneity) Lithostratigraphic units are therefore analogous toformations but are strictly informal Furthermore they are not de-fined by age geochemistry physical properties or paleontology al-though changes in these parameters may coincide with boundariesbetween lithostratigraphic units

Descriptive scheme for sediment and sedimentary rocksThe newly devised descriptive scheme (Figure F1) is divided

into four main sedimentary lithologic classes based on composi-tion volcanic nonvolcanic siliciclastic chemical and biogenic andmixed volcanic-siliciclastic or volcanic-biogenic with mixed re-ferred to as the tuffaceous lithologic class Within those lithologicclasses a principal name must be chosen the principal name isbased on particle size for the volcanic nonvolcanic siliciclastic andtuffaceous nonvolcanic siliciclastic lithologic classes In additionappropriate prefixes and suffixes may be chosen but this is optionalexcept for the prefix ldquotuffaceousrdquo for the tuffaceous lithologic classas described below

Sedimentary lithologic classesIn this section we describe lithologic classes and principal

names this is followed by a description of a new scheme where wedivide all particles into two size classes grains (lt2 mm) and clasts(gt2 mm) Then we describe prefixes and suffixes used in our newscheme and describe other parameters Volcaniclastic nonvolcanicsiliciclastic and chemical and biogenic sediment and rock can all bedescribed with equal precision in the new scheme presented here(Figure F1) The sedimentary lithologic classes based on types ofparticles are

bull Volcanic lithologic class defined as gt75 volcanic particlesbull Tuffaceous lithologic class containing 75ndash25 volcanic-de-

rived particles mixed with nonvolcanic particles (either or both nonvolcanic siliciclastic and chemical and biogenic)

bull Nonvolcanic siliciclastic lithologic class containing lt25 vol-canic siliciclastic particles and nonvolcanic siliciclastic particles dominate chemical and biogenic and

bull Biogenic lithologic class containing lt25 volcanic siliciclastic particles and nonvolcanic siliciclastic particles are subordinate to chemical and biogenic particles

The definition of the term tuffaceous (25ndash75 volcanic parti-cles) is modified from Fisher and Schmincke (1984) (Table T2)

Table T2 Relative abundances of volcanogenic material Volcanic component percentage are sensu stricto Fisher and Schmincke (1984) Components mayinclude volcanic glass pumice scoria igneous rock fragments and magmatic crystals Volcaniclastic lithology types modified from Fisher and Schmincke(1984) Bold = particle sizes are nonlithified (ie sediment) Download table in csv format

Volcaniccomponent

()Volcaniclasticlithology type Example A Example B

0ndash25 Sedimentary Sand sandstone Unconsolidated breccia consolidated breccia25ndash75 Tuffaceous Tuffaceous sand

tuffaceous sandstoneTuffaceous unconsolidated breccia tuffaceous

consolidated breccia75ndash100 Volcanic Ash tuff Unconsolidated volcanic breccia consolidated

volcanic breccia



Principal namesPrincipal names for sediment and sedimentary rock of the non-

volcanic siliciclastic and tuffaceous lithologic classes are adaptedfrom the grain size classes of Wentworth (1922) whereas principalnames for sediment and sedimentary rock of the volcanic lithologicclass are adapted from the grain size classes of Fisher andSchmincke (1984) (Table T3 Figure F3) Thus the Wentworth(1922) and Fisher and Schmincke (1984) classifications are used torefer to particle type (nonvolcanic versus volcanic respectively) andthe size of the particles (Figure F1) The principal name is thuspurely descriptive and does not depend on interpretations of frag-mentation transport depositional or alteration processes For eachgrain size class both a consolidated (ie semilithified to lithified)and a nonconsolidated term exists they are mutually exclusive (egmud or mudstone ash or tuff ) For simplicity Wentworthrsquos clay andsilt sizes are combined in a ldquomudrdquo class similarly fine medium andcoarse sand are combined in a ldquosandrdquo class

New definition of principal name conglomerate breccia-conglomerate and breccia

The grain size terms granule pebble and cobble (Wentworth1922) are replaced by breccia conglomerate or breccia-conglomer-ate in order to include critical information on the angularity of frag-ments larger than 2 mm (the sandgranule boundary of Wentworth1922) A conglomerate is defined as a deposit where the fragmentsare gt2 mm and are exclusively (gt95 vol) rounded and subrounded(Table T3 Figure F4) A breccia-conglomerate is composed of pre-dominantly rounded andor subrounded clasts (gt50 vol) and sub-ordinate angular clasts A breccia is predominantly composed ofangular clasts (gt50 vol) Breccia conglomerates and breccia-con-

glomerates may be consolidated (ie lithified) or unconsolidatedClast sphericity is not evaluated

Definition of grains versus clasts and detailed grain sizesWe use the general term ldquoparticlesrdquo to refer to the fragments that

make up volcanic tuffaceous and nonvolcanic siliciclastic sedimentand sedimentary rock regardless of the size of the fragments How-ever for reasons that are both meaningful and convenient we em-

Table T3 Particle size nomenclature and classifications Bold = particle sizes are nonlithified (ie sediments) Distinctive igneous rock clasts aredescribed in more detail as if they were igneous rocks Volcanic and nonvolcanic conglomerates and breccias are further described as clast supported(gt2 mm clasts dominantly in direct physical contact with each other) or matrix supported (gt2 mm clasts dominantly surrounded by lt2 mm diametermatrix infrequent clast-clast contacts) Download table in csv format

Particle size (mod Wentworth 1922)Diameter

(mm) Particle roundness Core description tips

Simplified volcanic equivalent(mod Fisher and Schmincke

1984)

Matrix Mud mudstone Clay claystone lt004 Not defined Particles not visible without microscope smooth to touch

lt2 mm particle diameter

Silt siltstone 004ndash063 Not defined Particles not visible with naked eye gritty to touch

Sand sandstone Fine sand fine sandstone 025ndash063 Not defined Particles visible with naked eye

Medium to coarse sand 025ndash2 Not defined Particles clearly visible with naked eye

Ash tuff

Medium to coarse sandstone

Clasts Unconsolidated conglomerate

Consolidated conglomerate

gt2 Exclusively rounded and subrounded clasts

Particle composition identifiable with naked eye or hand lens

2ndash64 mm particle diameterLapilli lapillistone

gt64 mm particle diameterUnconsolidated volcanic

conglomerateConsolidated volcanic

conglomerateUnconsolidated breccia-

conglomerateConsolidated breccia-

conglomerate

gt2 Angular clasts present with rounded clasts


Unconsolidated volcanic breccia-conglomerate

Consolidated volcanic breccia-conglomerate

Unconsolidated brecciaConsolidated breccia

gt2 Predominantly angular clasts Particle composition identifiable with naked eye or hand lens

Unconsolidated volcanic breccia

Consolidated volcanic breccia

Figure F3 Ternary diagram of volcaniclastic grain size terms and their associ-ated sediment and rock types (modified from Fisher and Schmincke 1984)

2575

2575

7525

7525

Lapilli-ashLapilli-tuff Ash

TuffLapilli

Lapillistone

Ash-breccia

Tuff-breccia

UnconsolidatedConsolidated


Volcanic conglomerate

Volcanic breccia-conglomerate

Volcanic breccia

Blocks and bombsgt64 mm

Lapilli2ndash64 mm

Ashlt2 mm


jim
Highlight
jim
Highlight
jim
Highlight


ploy a much stricter use of the terms ldquograinrdquo and ldquoclastrdquo for thedescription of these particles We refer to particles larger than 2 mmas clasts and particles smaller than 2 mm as grains This cut-off size(2 mm) corresponds to the sandgranule grain size division ofWentworth (1922) and the ashlapilli grain size divisions of Fisher(1961) Fisher and Schmincke (1984) Cas and Wright (1987) Mc-Phie et al (1993) and White and Houghton (2006) (Table T3) Thissize division has stood the test of time because it is meaningful par-ticles larger than 2 mm are much easier to see and describe macro-scopically (in core or on outcrop) than particles smaller than 2 mmAdditionally volcanic particles lt2 mm in size commonly includevolcanic crystals whereas volcanic crystals are virtually never gt2mm in size As examples using our definition an ash or tuff is madeentirely of grains a lapilli-tuff or tuff-breccia has a mixture of clastsand grains and a lapillistone is made entirely of clasts

Irrespective of the sediment or rock composition detailed aver-age and maximum grain size follows Wentworth (1922) For exam-ple an ash can be further described as sand-sized ash or silt-sizedash a lapilli-tuff can be described as coarse sand sized or pebblesized

Definition of prefix monomict versus polymictThe term mono- (one) when applied to clast compositions refers

to a single type and poly- (many) when applied to clast composi-tions refers to multiple types These terms have been most widelyapplied to clasts (gt2 mm in size eg conglomerates) because thesecan be described macroscopically We thus restrict our use of theterms monomict or polymict to particles gt2 mm in size (referred toas clasts in our scheme) and do not use the term for particles lt2 mmin size (referred to as grains in our scheme)

Variations within a single volcanic parent rock (eg a collapsinglava dome) may produce clasts referred to as monomict which areall of the same composition

Definition of prefix clast supported versus matrix supportedldquoMatrix supportedrdquo is used where smaller particles visibly en-

velop each of the larger particles The larger particles must be gt2mm in size that is they are clasts using our definition of the wordHowever the word ldquomatrixrdquo is not defined by a specific grain sizecutoff (ie it is not restricted to grains which are lt2 mm in size)For example a matrix-supported volcanic breccia could have blockssupported in a matrix of lapilli-tuff ldquoClast supportedrdquo is used whereclasts (gt2 mm in diameter) form the sediment framework in thiscase porosity and small volumes of matrix or cement are intersti-

tial These definitions apply to both macroscopic and microscopicobservations

Definition of prefix mafic versus evolved versus bimodalIn the scheme shown in Figure F1 the compositional range of

volcanic grains and clasts is represented by only three entriesldquomaficrdquo ldquobimodalrdquo and ldquoevolvedrdquo In macroscopic analysis maficversus evolved intervals are defined by the grayscale index of themain particle component with unaltered mafic grains and clastsusually ranging from black to dark gray and unaltered evolvedgrains and clasts ranging from dark gray to white Microscopic ex-amination may further aid in assigning the prefix mafic or evolvedusing glass shard color and mineralogy but precise determinationof bulk composition requires chemical analysis In general intervalsdescribed as mafic are inferred to be basalt and basaltic andesitewhereas intervals described as evolved are inferred to be intermedi-ate and silicic in composition but again geochemical analysis isneeded to confirm this Bimodal may be used where both mafic andevolved constituents are mixed in the same descriptive intervalCompositional prefixes (eg mafic evolved and bimodal) are op-tional and may be impossible to assign in altered rocks

In microscopic description a more specific compositional namecan be assigned to an interval if the necessary index minerals areidentified Following the procedures defined for igneous rocks (seebelow) the presence of olivine identifies the deposit as ldquobasalticrdquothe presence of quartz identifies the deposit as ldquorhyolite-daciterdquo andthe absence of both identifies the deposit as ldquoandesiticrdquo

SuffixesThe suffix is used for a subordinate component that deserves to

be highlighted It is restricted to a single term or phrase to maintaina short and effective lithology name containing the most importantinformation only It is always in the form ldquowith ashrdquo ldquowith clayrdquoldquowith foraminiferrdquo etc

Other parametersBed thicknesses (Table T4) follow the terminology of Ingram

(1954) but we group together thin and thick laminations into ldquolam-inardquo for all beds lt1 cm thick the term ldquoextremely thickrdquo is added forgt10 m thick beds Sorting and clast roundness values are restrictedto three terms well moderately and poor and rounded sub-rounded and angular respectively (Figure F4) for simplicity andconsistency between core describers

Intensity of bioturbation is qualified in four degrees noneslight moderate and strong corresponding to the degradation ofotherwise visible sedimentary structures (eg planar lamination)and inclusion of grains from nearby intervals

Macrofossil abundance is estimated in six degrees with domi-nant (gt50) abundant (2ndash50) common (5ndash20) rare (1ndash5) trace (lt1) and absent (Table T5) following common IODP

Figure F4 Visual representations of sorting and rounding classifications

Well sorted Moderately sorted Poorly sorted

Angular Subrounded Rounded

Sorting

Rounding

Table T4 Bed thickness classifications Download table in csv format

Layer thickness (cm)

Classification(mod Ingram 1954)

lt1 Lamina1ndash3 Very thin bed3ndash10 Thin bed10ndash30 Medium bed30ndash100 Thick bed100ndash1000 Very thickgt1000 Extremely thick



practice for smear slide stereomicroscopic and microscopic obser-vations The dominant macrofossil type is selected from an estab-lished IODP list

Quantification of the grain and clast componentry differs frommost previous Integrated Ocean Drilling Program (and equivalent)expeditions An assessment of grain and clast componentry in-cludes up to three major volcanic components (vitric crystal andlithic) which are sorted by their abundance (ldquodominantrdquo ldquosecondorderrdquo and ldquothird orderrdquo) The different types of grains and clastsoccurring within each component type are listed below

Vitric grains (lt2 mm) and clasts (gt2 mm) can be angular sub-rounded or rounded and of the following types

bull Pumicebull Scoriabull Shardsbull Glass densebull Pillow fragmentbull Accretionary lapillibull Fiammebull Limu o Pelebull Pelersquos hair (microscopic only)

Crystals can be euhedral subhedral or anhedral and are alwaysdescribed as grains regardless of size (ie they are not clasts) theyare of the following types

bull Olivinebull Quartzbull Feldsparbull Pyroxenebull Amphibolebull Biotitebull Opaquebull Other

Lithic grains (lt2 mm) and clasts (gt2 mm) can be angular sub-rounded or rounded and of the following types (igneous plutonicgrains do not occur)

bull Igneous clastgrain mafic (unknown if volcanic or plutonic)bull Igneous clastgrain evolved (unknown if volcanic or plutonic)bull Volcanic clastgrain evolvedbull Volcanic clastgrain maficbull Plutonic clastgrain maficbull Plutonic clastgrain evolvedbull Metamorphic clastgrain

bull Sandstone clastgrainbull Carbonate clastgrain (shells and carbonate rocks)bull Mudstone clastgrainbull Plant remains

In macroscopic description matrix can be well moderately orpoorly sorted based on visible grain size (Figure F3) and of the fol-lowing types

bull Vitricbull Crystalbull Lithicbull Carbonatebull Other

SummaryWe have devised a new scheme to improve description of volca-

niclastic sediments and their mixtures with nonvolcanic (siliciclas-tic chemogenic and biogenic) particles while maintaining theusefulness of prior schemes for describing nonvolcanic sedimentsIn this scheme inferred fragmentation transport and alterationprocesses are not part of the lithologic name Therefore volcanicgrains inferred to have formed by a variety of processes (ie pyro-clasts autoclasts epiclasts and reworked volcanic clasts Fisher andSchmincke 1984 Cas and Wright 1987 McPhie et al 1993) aregrouped under a common grain size term that allows for a more de-scriptive (ie nongenetic) approach than proposed by previous au-thors However interpretations can be entered as comments in thedatabase these may include inferences regarding fragmentationprocesses eruptive environments mixing processes transport anddepositional processes alteration and so on

Igneous rocksIgneous rock description procedures during Expedition 350

generally followed those used during previous Integrated OceanDrilling Program expeditions that encountered volcaniclastic de-posits (eg Expedition 330 Scientists 2012 Expedition 336 Scien-tists 2012 Expedition 340 Scientists 2013) with modifications inorder to describe multiple clast types at any given interval Macro-scopic observations were coordinated with thin section or smearslide petrographic observations and bulk-rock chemical analyses ofrepresentative samples Data for the macroscopic and microscopicdescriptions of recovered cores were entered into the LIMS data-base using the DESClogik program

During Expedition 350 we recovered volcaniclastic sedimentsthat contain igneous particles of various sizes as well as an igneousunit classified as an intrusive sheet Therefore we describe igneousrocks as either a coherent igneous body or as large igneous clasts involcaniclastic sediment If igneous particles are sufficiently large tobe described individually at the macroscopic scale (gt2 cm) they aredescribed for lithology with prefix and suffix texture grain sizeand contact relationships in the extrusive_hypabyssal and intru-sive_mantle tabs in DESClogik In thin section particles gt2 mm insize are described as individual clasts or as a population of clastsusing the 2 mm size cutoff between grains and clasts describedabove this is a suitable size at the scale of thin section observation(Figure F5)

Plutonic rocks are holocrystalline (100 crystals with all crys-tals gt10 mm) with crystals visible to the naked eye Volcanic rocks

Table T5 Macrofossil abundance classifications Download table in csvformat

Macrofossil abundance

(vol) Classification

0 Absentlt1 Trace1ndash5 Rare5ndash20 Common20ndash50 Abundantgt50 Dominant



are composed of a glassy or microcrystalline groundmass (crystalslt10 mm) and can contain various proportions of phenocrysts (typ-ically 5 times larger than groundmass usually gt01 mm) andor ves-icles

UnitsIgneous rocks are described at the level of the descriptive inter-

val (the individual descriptive line in DESClogik) the lithologicunit and ultimately at the level of the lithostratigraphic unit A de-scriptive interval consists of variations in rock characteristics suchas vesicle distribution igneous textures mineral modes and chilledmargins Rarely a descriptive interval may comprise multiple do-mains for example in the case of mingled magmas Lithologic unitsin coherent igneous bodies are defined either by visual identifica-tion of actual lithologic contacts (eg chilled margins) or by infer-ence of the position of such contacts using observed changes inlithology (eg different phenocryst assemblage or volcanic fea-tures) These lithologic units can include multiple descriptive inter-vals The relationship between multiple lithologic units is then usedto define an overall lithostratigraphic interval

Volcanic rocksSamples within the volcanic category are massive lava pillow

lava intrusive sheets (ie dikes and sills) volcanic breccia inti-mately associated with lava flows and volcanic clasts in sedimentand sedimentary rock (Table T6) Volcanic breccia not associatedwith lava flows and hyaloclastites not associated with pillow lava aredescribed in the sediment tab in DESClogik Monolithic volcanicbreccia with clast sizes lt64 cm (minus6φ) first encountered beneath anyother rock type are automatically described in the sediment tab inorder to avoid confusion A massive lava is defined as a coherentvolcanic body with a massive core and vesiculated (sometimes brec-ciated or glassy) flow top and bottom When possible we identifypillow lava on the basis of being subrounded massive volcanic bod-ies (02ndash1 m in diameter) with glassy margins (andor broken glassyfragments hereby described as hyaloclastite) that commonly showradiating fractures and decreasing mineral abundances and grainsize toward the glassy rims The pillow lava category therefore in-cludes multiple seafloor lava flow morphologies (eg sheet lobatehackly etc) Intrusive sheets are defined as dikes or sills cuttingacross other lithologic units They consist of a massive core with aholocrystalline groundmass and nonvesiculated chilled margins

along their boundaries Their size varies from several millimeters toseveral meters in thickness Clasts in sediment include both lithic(dense) and vitric (inflated scoria and pumice) varieties

LithologyVolcanic rocks are usually classified on the basis of their alkali

and silica contents A simplified classification scheme based on vi-sual characteristics is used for macroscopic and microscopic deter-minations The lithology name consists of a main principal nameand optional prefix and suffix (Table T6) The main lithologic namedepends on the nature of phenocryst minerals andor the color ofthe groundmass Three rock types are defined for phyric samples

bull Basalt black to dark gray typically olivine-bearing volcanic rock

bull Andesite dark to light gray containing pyroxenes andor feld-spar andor amphibole typically devoid of olivine and quartz and

bull Rhyolite-dacite light gray to pale white usually plagioclase-phy-ric and sometimes containing quartz plusmn biotite this macroscopic category may extend to SiO2 contents lt70 and therefore may include dacite

Volcanic clasts smaller than the cutoff defined for macroscopic(2 cm) and microscopic (2 mm) observations are described only asmafic (dark-colored) or evolved (light-colored) in the sediment tabDark aphyric rocks are considered to be basalt whereas light-col-ored aphyric samples are considered to be rhyolite-dacite with theexception of obsidian (generally dark colored but rhyolitic in com-position)

The prefix provides information on the proportion and the na-ture of phenocrysts Phenocrysts are defined as crystals signifi-cantly larger (typically 5 times) than the average size of thegroundmass crystals Divisions in the prefix are based on total phe-nocryst proportions

bull Aphyric (lt1 phenocrysts)bull Sparsely phyric (ge1ndash5 phenocrysts)bull Moderately phyric (gt5ndash20 phenocrysts)bull Highly phyric (gt20 phenocrysts)

The prefix also includes the major phenocryst phase(s) (iethose that have a total abundance ge1) in order of increasing abun-dance left to right so the dominant phase is listed last Macroscopi-cally pyroxene and feldspar subtypes are not distinguished butmicroscopically they are identified as orthopyroxene and clinopy-roxene and plagioclase and K-feldspar respectively Aphyric rocksare not given any mineralogical identifier

The suffix indicates the nature of the volcanic body massivelava pillow lava intrusive sheet or clast In rare cases the suffix hy-aloclastite or breccia is used if the rock occurs in direct associationwith a related in situ lava (Table T6) As mentioned above thicksections of hyaloclastite or breccia unrelated to lava are described inthe sediment tab

Plutonic rocksPlutonic rocks are classified according to the IUGS classification

of Le Maitre et al (2002) The nature and proportion of minerals areused to give a root name to the sample (see Figure F6 for the rootnames used) A prefix can be added to indicate the presence of amineral not present in the definition of the main name (eg horn-

Figure F5 A Tuff composed of glass shards and crystals described as sedi-ment in DESClogik (350-U1437D-38R-2 TS20) B Lapilli-tuff containing pum-ice clasts in a glass and crystal matrix (29R TS10) The matrix and clasts aredescribed as sediment and the vitric and lithic clasts (gt2 mm) are addition-ally described as extrusive or intrusive as appropriate Individual clasts or apopulation of clasts can be described together

A B

PumicePumice

1 mm 1 mm



blende-tonalite) or to emphasize a special textural feature (eg lay-ered gabbro) Mineral prefixes are listed in order of increasingabundance left to right

Leucocratic rocks dominated by quartz and feldspar are namedusing the quartzndashalkali feldsparndashplagioclase (Q-A-P) diagram of LeMaitre et al (2002) (Figure F6A) For example rocks dominated byplagioclase with minor amounts of quartz K-feldspar and ferro-magnesian silicates are diorite tonalites are plagioclase-quartz-richassemblages whereas granites contain quartz K-feldspar and plagi-oclase in similar proportions For melanocratic plutonic rocks weused the plagioclase-clinopyroxene-orthopyroxene triangular plotsand the olivine-pyroxenes-plagioclase triangle (Le Maitre et al2002) (Figure F6B)

TexturesTextures are described macroscopically for all igneous rock core

samples but a smaller subset is described microscopically in thinsections or grain mounts Textures are discriminated by averagegrain size (groundmass for porphyritic rocks) grain size distribu-tion shape and mutual relations of grains and shape-preferred ori-entation The distinctions are based on MacKenzie et al (1982)

Textures based on groundmass grain size of igneous rocks aredefined as

bull Coarse grained (gt5ndash30 mm)bull Medium grained (gt1ndash5 mm)bull Fine grained (gt05ndash1 mm)bull Microcrystalline (01ndash05 mm)

In addition for microscopic descriptions cryptocrystalline (lt01mm) is used The modal grain size of each phenocryst phase is de-scribed individually

For extrusive and hypabyssal categories rock is described as ho-locrystalline glassy (holohyaline) or porphyritic Porphyritic tex-ture refers to phenocrysts or microphenocrysts surrounded bygroundmass of smaller crystals (microlites le 01 mm Lofgren 1974)or glass Aphanitic texture signifies a fine-grained nonglassy rockthat lacks phenocrysts Glomeroporphyritic texture refers to clus-ters of phenocrysts Magmatic flow textures are described as tra-chytic when plagioclase laths are subparallel Spherulitic texturesdescribe devitrification features in glass whereas perlite describes

Figure F6 Classification of plutonic rocks following Le Maitre et al (2002)A Q-A-P diagram for leucocratic rocks B Plagioclase-clinopyroxene-ortho-pyroxene triangular plots and olivine-pyroxenes-plagioclase triangle formelanocratic rocks

Q

PA

90

60

20

5

90653510

Quartzolite

Granite

Monzogranite

Sye

nogr

anite

Quartz monozite

Syenite Monzonite

Granodiorite

Tonalite

Alka

li fe

ldsp

ar g

rani

te

Alkali feldspar syenite

A

Plagioclase

Plagioclase PlagioclaseOlivine

Orthopyroxene

Norite

NoriteW

ehrlite

Olivine

Clinopyroxenite

Oliv

ine

orth

opyr

oxen

ite

Har

zbur

gite

Gab

bro

Gab

bro

Olivine gabbro Olivine norite

Troctolite TroctoliteDunite

Lherzolite

Anorthosite Anorthosite

Clinopyroxenite

Orthopyroxenite

Websterite

Gabbronorite

40

Clin

opyr

oxen

e

Anorthosite90

5

B

Quartz diorite Quartz gabbro Quartz anorthosite

Quartz syenite Quartz monzodiorite Quartz monzogabbro

Monzodiorite Monzogabbro

DioriteGabbro

Anorthosite

Quartz alkalifeldspar syenite

Quartz-richgranitoids

Olivinewebsterite

Table T6 Explanation of nomenclature for extrusive and hypabyssal volcanic rocks Download table in csv format

Prefix Main name Suffix

1st of phenocrysts 2nd relative abundance of phenocrysts

If phyric

Aphyric (lt1) Sorted by increasing abundance from left to right separated by hyphens

Basalt black to dark gray typically olivine-bearing volcanic rock

Massive lava massive core brecciated or vesiculated flow top and bottom gt1 m thick

Sparsely phyric (1ndash5) Andesite dark to light gray contains pyroxenes andor feldspar andor amphibole and is typically devoid of olivine and quartz

Pillow lava subrounded bodies separated by glassy margins andor hyaloclastite with radiating fractures 02 to 1 m wide

Moderately phyric (5ndash20) Rhyolite-dacite light gray to pale white andor quartz andor biotite-bearing volcanic rock

Intrusive sheet dyke or sill massive core with unvesiculated chilled margin from millimeters to several meters thick

Highly phyric (gt20) Lithic clast pumice clast scoria clast volcanic or plutonic lapilli or blocks gt2 cm to be defined as sample domain

If aphyric Hyaloclastite breccia made of glassy fragments

Basalt dark colored Breccia

Rhyolite light colored



rounded hydration fractures in glass Quench margin texture de-scribes a glassy or microcrystalline margin to an otherwise coarsergrained interior Individual mineral percentages and sizes are alsorecorded

Particular attention is paid to vesicles as they might be a majorcomponent of some volcanic rocks However they are not includedin the rock-normalized mineral abundances Divisions are made ac-cording to proportions

bull Not vesicular (le1 vesicles)bull Sparsely vesicular (gt1ndash10 vesicles)bull Moderately vesicular (gt10ndash40 vesicles)bull Highly vesicular (gt40 vesicles)

The modal shape and sphericity of vesicle populations are esti-mated using appropriate comparison charts following Expedition330 Scientists (2012) (Figure F7)

For intrusive rocks (all grains gt1 mm) macroscopic textures aredivided into equigranular (principal minerals have the same rangein size) and inequigranular (the principal minerals have differentgrain sizes) Porphyritic texture is as described above for extrusiverocks Poikilitic texture is used to describe larger crystals that en-close smaller grains We also use the terms ophitic (olivine or pyrox-ene partially enclose plagioclase) and subophitic (plagioclasepartially enclose olivine or pyroxene) Crystal shapes are describedas euhedral (the characteristic crystal shape is clear) subhedral(crystal has some of its characteristic faces) or anhedral (crystallacks any characteristic faces)

AlterationSubmarine samples are likely to have been variably influenced

by alteration processes such as low-temperature seawater alter-ation therefore the cores and thin sections are visually inspectedfor alteration

Macroscopic core descriptionThe influence of alteration is determined during core descrip-

tion Descriptions span alteration of minerals groundmass orequivalent matrix volcanic glass pumice scoria rock fragmentsand vesicle fill The color is used as a first-order indicator of alter-ation based on a simple color scheme (brown green black graywhite and yellow) The average extent of secondary replacement ofthe original groundmass or matrix is used to indicate the alterationintensity for a descriptive interval per established IODP values

Slight = lt10Moderate = 10ndash50High = gt50

The alteration assemblages are described as dominant second-order and third-order phases replacing the original minerals withinthe groundmass or matrix Alteration of glass at the macroscopiclevel is described in terms of the dominant phase replacing the glassGroundmass or matrix alteration texture is described as pseudo-morphic corona patchy and recrystallized For patchy alterationthe definition of a patch is a circular or highly elongate area of alter-ation described in terms of shape as elongate irregular lensoidallobate or rounded and the dominant phase of alteration in thepatches The most common vesicle fill compositions are reported asdominant second-order and third-order phases

Vein fill and halo mineralogy are described with the dominantsecond-order and third-order hierarchy Halo alteration intensity isexpressed by the same scale as for groundmass alteration intensityFor veins and halos it is noted that the alteration mineralogy of ha-los surrounding the veins can affect both the original minerals oroverprint previous alteration stages Veins and halos are also re-corded as density over a 10 cm core interval


Microscopic descriptionCore descriptions of alteration are followed by thin section

petrography The intensity of replacement of original rock compo-nents is based on visual estimations of proportions relative to totalarea of the thin section Descriptions are made in terms of domi-nant second-order and third-order replacing phases for mineralsgroundmassmatrix clasts glass and patches of alteration whereasvesicle and void fill refer to new mineral phases filling the spacesDescriptive terms used for alteration extent are


Alteration of the original minerals and groundmass or matrix isdescribed in terms of the percentage of the original phase replacedand a breakdown of the replacement products by percentage of thealteration Comments are used to provide further specific informa-tion where available Accurate identification of very fine-grainedminerals is limited by the lack of X-ray diffraction during Expedi-tion 350 therefore undetermined clay mineralogy is reported asclay minerals

VCD standard graphic summary reportsStandard graphic reports were generated from data downloaded

from the LIMS database to summarize each core (typical for sedi-ments) or section half (typical for igneous rocks) An example VCDfor lithostratigraphy is shown in Figure F8 Patterns and symbolsused in VCDs are shown in Figures F9 and F10

Figure F7 Classification of vesicle sphericity and roundness (adapted fromthe Wentworth [1922] classification scheme for sediment grains)

Sphericity

High

Moderate

Low

Elongate

Pipe

Rounded

Subrounded

Subangular

Angular

Very angular

Roundness



Figure F8 Example of a standard graphic summary showing lithostratigraphic information

mio

cene

VI

1

2

3

4

5

6

7

0

100

200

300

400

500

600

700

800

900137750

137650

137550

137450

137350

137250

137150

137050

136950pumice

pumice

pumice

fiamme

pillow fragment

fiamme

fiamme

fiamme

pumicefiamme

pumice

pumice

pumice

XRF

TSBTS

MAD

HS

MAD

MAD

MAD

10-40

20-80

ReflectanceL a b

600200 Naturalgammaradiation

(cps)

40200

MS LoopMS Point

(SI)

20000

Age

Ship

boar

dsa

mpl

es

Sedi

men

tary

stru

ctur

es

Graphiclithology

CoreimageLi

thol

ogic

unit

Sect

ion

Core

leng

th (c

m)

Dept

h CS

F-A

(m)

Hole 350-U1437E Core 33R Interval 13687-137802 m (CSF-A)

Dist

urba

nce

type

lapilli-tuff intercalated with tuff and tuffaceous mudstone

Dom

inan

t vitr

ic

Grain size rankMax

Modal

1062

Gra

ding

Dom

inan

t

2nd

orde

r

3rd

orde

r

Component

Clos

ely

inte

rcal

ated



GeochemistryHeadspace analysis of hydrocarbon gasesOne sample per core was routinely subjected to headspace hy-

drocarbon gas analysis as part of the standard shipboard safetymonitoring procedure as described in Kvenvolden and McDonald(1986) to ensure that the sediments being drilled do not containgreater than the amount of hydrocarbons that is safe to operatewith Therefore ~3ndash5 cm3 of sediment was collected from freshlyexposed core (typically at the end of Section 1 of each core) directlyafter it was brought on deck The extracted sediment sample wastransferred into a 20 mL headspace glass vial which was sealed withan aluminum crimp cap with a teflonsilicon septum and subse-quently put in an oven at 70degC for 30 min allowing the diffusion ofhydrocarbon gases from the sediment For subsequent gas chroma-tography (GC) analysis an aliquot of 5 cm3 of the evolved hydrocar-bon gases was extracted from the headspace vial with a standard gassyringe and then manually injected into the AgilentHewlett Pack-ard 6890 Series II gas chromatograph (GC3) equipped with a flameionization detector set at 250degC The column used for the describedanalysis was a 24 m long (2 mm inner diameter 63 mm outer di-

Figure F9 Lithology patterns and definitions for standard graphic summaries

Finesand

Granule Pebble CobbleSiltClay

Mud Sand Gravel

ClayClaystone

MudMudstone

100001

90002

80004

70008

60016

50031

40063

30125

20250

10500

01

-12

-24

-38

-416

-532

-664

-7128

-8256

-9512

Φmm

AshLapilli

Volcanic brecciaVolcanic conglomerate


SandSandstone

Evolved ashTuff

Tuffaceous sandSandstone

Bimodal ashTuff

Rhyoliteor

dacite

Finegrained Medium grainedMicrocrystalline Coarse grained

Tuffaceous mudMudstone

Mafic ashTuff

Monomicticbreccia

Polymictic evolvedlapilli-ashTuff

Polymictic evolvedlapilliLapillistone

Foraminifer oozeChalk

Evolved

Mafic

Clast-supported Matrix-supported Clast-supported

Fine ash Coarse ash

Very finesand

Mediumsand

Coarsesand

Very coarsesand

Boulder

Polymictic

Monomictic

Polymictic

Monomictic

Polymictic

Monomictic

Polymictic

Monomictic

Intermediateor

bimodal

Polymictic evolvedvolcanic breccia

Polymictic intermediatevolcanic breccia

Polymicticbreccia-conglomerate

Polymicticbreccia

Monomictic evolvedlapilli-ashTuff

Polymictic intermediatelapilli-ashTuff

Polymictic intermediatelapilliLapillistone

Monomictic intermediatelapilli-ashTuff

Polymictic maficlapilli-ashTuff

Monomictic maficlapilli-ashTuff

Monomictic evolvedlapilliLapillistone

Polymictic maficlapilliLapillistone

Monomictic maficlapilliLapillistone

Tuffaceous breccia

Polymictic evolvedashTuff-breccia

Evolved monomicticashTuff-breccia

Figure F10 Symbols used on standard graphic summaries

Disturbance type

Basal flow-in

Biscuit

Brecciated

Core extension

Fall-in

Fractured

Mid-core flow-in

Sediment flowage

Soupy

Void

Component

Lithic

Crystal

Vitric

Sedimentary structure

Convolute bedded

Cross-bedded

Flame structure

Intraclast

Lenticular bedded

Soft sediment deformation

Stratified

Grading

Density graded

Normally graded

Reversely graded



ameter) column packed with 80100 mesh HayeSep (Restek) TheGC3 oven program was set to hold at 80degC for 825 min with subse-quent heat-up to 150degC at 40degCmin The total run time was 15 min

Results were collected using the Hewlett Packard 3365 Chem-Station data processing software The chromatographic responsewas calibrated to nine different analysis gas standards and checkedon a daily basis The concentration of the analyzed hydrocarbongases is expressed as parts per million by volume (ppmv)

Pore fluid analysisPore fluid collection

Whole-round core samples generally 5 cm long and in somecases 10 cm long (RCB cores) were cut immediately after the corewas brought on deck capped and taken to the laboratory for porefluid processing Samples collected during Expedition 350 wereprocessed under atmospheric conditions After extrusion from thecore liner contamination from seawater and sediment smearingwas removed by scraping the core surface with a spatula In APCcores ~05 cm of material from the outer diameter and the top andbottom faces was removed whereas in XCB and RCB cores whereborehole contamination is higher as much as two-thirds of the sed-iment was removed from each whole round The remaining ~150ndash300 cm3 inner core was placed into a titanium squeezer (modifiedafter Manheim and Sayles 1974) and compressed using a laboratoryhydraulic press The squeezed pore fluids were filtered through aprewashed Whatman No 1 filter placed in the squeezers above atitanium mesh screen Approximately 20 mL of pore fluid was col-lected in precleaned plastic syringes attached to the squeezing as-sembly and subsequently filtered through a 045 μm Gelmanpolysulfone disposable filter In deeper sections fluid recovery wasas low as 5 mL after squeezing the sediment for as long as ~2 h Af-ter the fluids were extracted the squeezer parts were cleaned withshipboard water and rinsed with deionized (DI) water Parts weredried thoroughly prior to reuse

Sample allocation was determined based on the pore fluid vol-ume recovered and analytical priorities based on the objectives ofthe expedition Shipboard analytical protocols are summarized be-low

Shipboard pore fluid analysesPore fluid samples were analyzed on board the ship following

the protocols in Gieskes et al (1991) Murray et al (2000) and theIODP user manuals for newer shipboard instrumentation Precisionand accuracy was tested using International Association for thePhysical Science of the Ocean (IAPSO) standard seawater with thefollowing reported compositions alkalinity = 2353 mM Cl = 5596mM sulfate = 2894 mM Na = 4807 mM Mg = 541 mM K = 1046mM Ca = 1054 mM Li = 264 μM B = 450 μM and Sr = 93 μM(Gieskes et al 1991 Millero et al 2008 Summerhayes and Thorpe1996) Pore fluid components reported here that have low abun-dances in seawater (ammonium phosphate Mn Fe Ba and Si) arebased on calibrations using stock solutions (Gieskes et al 1991)

Alkalinity pH and salinityAlkalinity and pH were measured immediately after squeezing

following the procedures in Gieskes et al (1991) pH was measuredwith a combination glass electrode and alkalinity was determinedby Gran titration with an autotitrator (Metrohm 794 basic Titrino)using 01 M HCl at 20degC Certified Reference Material 104 obtainedfrom the laboratory of Andrew Dickson (Marine Physical Labora-tory Scripps Institution of Oceanography USA) was used for cali-bration of the acid IAPSO standard seawater was used for

calibration and was analyzed at the beginning and end of a set ofsamples for each site and after every 10 samples Salinity was subse-quently measured using a Fisher temperature-compensated hand-held refractometer

ChlorideChloride concentrations were acquired directly after pore fluid

squeezing using a Metrohm 785 DMP autotitrator and silver nitrate(AgNO3) solutions that were calibrated against repeated titrationsof IAPSO standard Where fluid recovery was ample a 05 mL ali-quot of sample was diluted with 30 mL of HNO3 solution (92 plusmn 2mM) and titrated with 01015 M AgNO3 In all other cases a 01 mLaliquot of sample was diluted with 10 mL of 90 plusmn 2 mM HNO3 andtitrated with 01778 M AgNO3 IAPSO standard solutions analyzedinterspersed with the unknowns are accurate and precise to lt5

Sulfate bromide sodium magnesium potassium and calciumAnion (sulfate and Br) and cation (Na Mg K and Ca) abun-

dances were analyzed using a Metrohm 850 ion chromatographequipped with a Metrohm 858 Professional Sample Processor as anautosampler Cl concentrations were also determined in the ionchromatography (IC) analyses but are only considered here forcomparison because the titration values are generally more reliableThe eluent solutions used were diluted 1100 with DI water usingspecifically designated pipettes The analytical protocol was to es-tablish a seawater standard calibration curve using IAPSO dilutionsof 100times 150times 200times 350times and 500times Reproducibility for IAPSOanalyses by IC interspersed with the unknowns are Br = 29 Cl =05 sulfate = 06 Ca = 49 Mg = 12 K = 223 and Na =05 (n = 10) The deviations of the average concentrations mea-sured here relative to those in Gieskes et al (1991) are Br = 08 Cl= 01 sulfate = 03 Ca = 41 Mg = 08 K = minus08 and Na =03

Ammonium and phosphateAmmonium concentrations were determined by spectrophoto-

metry using an Agilent Technologies Cary Series 100 ultraviolet-visible spectrophotometer with a sipper sample introduction sys-tem following the protocol in Gieskes et al (1991) Samples were di-luted prior to color development so that the highest concentrationwas lt1000 μM Phosphate was measured using the ammoniummolybdate method described in Gieskes et al (1991) using appro-priate dilutions Relative uncertainties of ammonium and phos-phate determinations are estimated at 05ndash2 and 08respectively (Expedition 323 Scientists 2011)

Major and minor elements (ICP-AES)Major and minor elements were analyzed by inductively cou-

pled plasmandashatomic emission spectroscopy (ICP-AES) with a Tele-dyne Prodigy high-dispersion ICP spectrometer The generalmethod for shipboard ICP-AES analysis of samples is described inOcean Drilling Program (ODP) Technical Note 29 (Murray et al2000) and the user manuals for new shipboard instrumentationwith modifications as indicated (Table T7) Samples and standardswere diluted 120 using 2 HNO3 spiked with 10 ppm Y for traceelement analyses (Li B Mn Fe Sr Ba and Si) and 1100 for majorconstituent analyses (Na K Mg and Ca) Each batch of samples runon the ICP spectrometer contains blanks and solutions of known

Table T7 Primary secondary and tertiary wavelengths used for rock andinterstitial water measurements by ICP-AES Expedition 350 Downloadtable in csv format



concentrations Each item aspirated into the ICP spectrometer wascounted four times from the same dilute solution within a givensample run Following each instrument run the measured raw in-tensity values were transferred to a data file and corrected for in-strument drift and blank If necessary a drift correction was appliedto each element by linear interpolation between the drift-monitor-ing solutions

Standardization of major cations was achieved by successive di-lution of IAPSO standard seawater to 120 100 75 50 2510 5 and 25 relative to the 1100 primary dilution ratio Repli-cate analyses of 100 IAPSO run as an unknown throughout eachbatch of analyses yielded estimates for precision and accuracy

For minor element concentration analyses the interstitial watersample aliquot was diluted by a factor of 20 (05 mL sample added to95 mL of a 10 ppm Y solution) Because of the high concentrationof matrix salts in the interstitial water samples at a 120 dilutionmatrix matching of the calibration standards is necessary to achieveaccurate results by ICP-AES A matrix solution that approximatedIAPSO standard seawater major ion concentrations was preparedaccording to Murray et al (2000) A stock standard solution wasprepared from ultrapure primary standards (SPC Science Plasma-CAL) in 2 nitric acid solution The stock solution was then dilutedin the same 2 ultrapure nitric acid solution to concentrations of100 75 50 25 10 5 and 1 The calibration standardswere then diluted using the same method as for the samples for con-sistency All calibration standards were analyzed in triplicate with areproducibility of Li = 083 B = 125 Si = 091 and Sr = 083IAPSO standard seawater was also analyzed as an unknown duringthe same analytical session to check for accuracy Relative devia-tions are Li = +18 B = 40 Si = 41 and Sr = minus18 Becausevalues of Ba Mn and Fe in IAPSO standard seawater are close to orbelow detection limits the accuracy of the ICP-AES determinationscannot be quantified and reported values should be regarded aspreliminary

Sediment bulk geochemistryFor shipboard bulk geochemistry analysis sediment samples

comprising 5 cm3 were taken from the interiors of cores with auto-claved cut-tip syringes freeze-dried for ~24 h to remove water andpowdered to ensure homogenization Carbonate content was deter-mined by acidifying approximately 10 mg of bulk powder with 2 MHCl and measuring the CO2 evolved all of which was assumed to bederived from CaCO3 using a UIC 5011 CO2 coulometer Theamounts of liberated CO2 were determined by trapping the CO2with ethanolamine and titrating coulometrically the hydroxyethyl-carbamic acid that is formed The end-point of the titration was de-termined by a photodetector The weight percent of total inorganiccarbon was calculated by dividing the CaCO3 content in weight per-cent by 833 the stoichiometric factor of C in CaCO3

Total carbon (TC) and total nitrogen (TN) contents were deter-mined by an aliquot of the same sample material by combustion atgt900degC in a Thermo Electron FlashEA 1112 elemental analyzerequipped with a Thermo Electron packed column and a thermalconductivity detector (TCD) Approximately 10 mg powder wasweighed into a tin cup and subsequently combusted in an oxygengas stream at 900degC for TC and TN analysis The reaction gaseswere passed through a reduction chamber to reduce nitrogen oxidesto N2 and the mixture of CO2 and N2 was separated by GC and de-tected by the TCD Calibration was based on the Thermo FisherScientific NC Soil Reference Material standard which contains 229wt C and 021 wt N The standard was chosen because its ele-

mental concentrations are equivalent to those encountered at SiteU1437 Relative uncertainties are 1 and 2 for TC and TN deter-minations respectively (Expedition 323 Scientists 2011) Total or-ganic carbon content was calculated by subtracting weight percentof inorganic carbon derived from the carbonate measured by coulo-metric analysis from total C obtained with the elemental analyzer

Sampling and analysis of igneous and volcaniclastic rocks

Reconnaissance analysis by portable X-ray fluorescence spectrometer

Volcanic rocks encountered during Expedition 350 show a widerange of compositions from basalt to rhyolite and the desire to rap-idly identify compositions in addition to the visual classification ledto the development of reconnaissance analysis by portable X-rayfluorescence (pXRF) spectrometry For this analysis a Thermo-Ni-ton XL3t GOLDD+ instrument equipped with an Ag anode and alarge-area drift detector for energy-dispersive X-ray analysis wasused The detector is nominally Peltier cooled to minus27degC which isachieved within 1ndash2 min after powering up During operation how-ever the detector temperature gradually increased to minus21degC overrun periods of 15ndash30 min after which the instrument needed to beshut down for at least 30 min This faulty behavior limited samplethroughput but did not affect precision and accuracy of the dataThe 8 mm diameter analysis window on the spectrometer is coveredby 3M thin transparent film and can be purged with He gas to en-hance transmission of low-energy X-rays X-ray ranges and corre-sponding filters are preselected by the instrument software asldquolightrdquo (eg Mg Al and Si) ldquolowrdquo (eg Ca K Ti Mn and Fe)ldquomainrdquo (eg Rb Sr Y and Zr) and ldquohighrdquo (eg Ba and Th) Analyseswere performed on a custom-built shielded stand located in theJOIDES Resolution chemistry lab and not in portable mode becauseof radiation safety concerns and better analytical reproducibility forpowdered samples

Two factory-set modes for spectrum quantification are availablefor rock samples ldquosoilrdquo and ldquominingrdquo Mining uses a fundamentalparameter calibration taking into account the matrix effects from allidentified elements in the analyzed spectrum (Zurfluh et al 2011)In soil mode quantification is performed after dividing the base-line- and interference-corrected intensities for the peaks of interestto those of the Compton scatter peak and then comparing thesenormalized intensities to those of a suitable standard measured inthe factory (Zurfluh et al 2011) Precision and accuracy of bothmodes were assessed by analyzing volcanic reference materials(Govindaraju 1994) In mining mode light elements can be ana-lyzed when using the He purge but the results obtained during Ex-pedition 350 were generally deemed unreliable The inability todetect abundant light elements (mainly Na) and the difficulty ingenerating reproducible packing of the powders presumably biasesthe fundamental parameter calibration This was found to be partic-ularly detrimental to the quantification of light elements Mg Aland Si The soil mode was therefore used for pXRF analysis of coresamples

Spectrum acquisition was limited to the main and low-energyrange (30 s integration time each) because elements measured inthe high mode were generally near the limit of detection or unreli-able No differences in performance were observed for main andlow wavelengths with or without He purge and therefore analyseswere performed in air for ease of operation For all elements the fac-tory-set soil calibration was used except for Y which is not re-ported by default To calculate Y abundances the main energy



spectrum was exported and background-subtracted peak intensi-ties for Y Kα were normalized to the Ag Compton peak offline TheRb Kβ interference on Y Kα was then subtracted using the approachin Gaacutesquez et al (1997) with a Rb KβRb Kα factor of 011 deter-mined from regression of Standards JB-2 JB-3 BHVO-2 and BCR-2 (basalts) AGV-1 and JA-2 (andesites) JR-1 and JR-2 (rhyolite)and JG-2 (granite) A working curve determined by regression of in-terference-corrected Y Kα intensities versus Y concentration wasestablished using the same rock standards (Figure F11)

Reproducibility was estimated from replicate analyses of JB-2standard (n = 131) and was found to be lt5 (1σ relative error) forindicator elements K Ca Sr Y and Zr over an ~7 week period (Fig-ure F12 Table T8) No instrumental drift was observed over thisperiod Accuracy was evaluated by analyzing Standards JB-2 JB-3BHVO-2 BCR-2 AGV-1 JA-2 and JR-1 in replicate Relative devi-ations from the certified values (Figure F13) are generally within20 (relative) For some elements deviations correlate with changesin the matrix composition (eg from basalt to rhyolite deviationsrange from Ca +2 to minus22) but for others (eg K and Zr) system-atic trends with increasing SiO2 are absent Zr abundances appearto be overestimated in high-Sr samples likely because of the factory-calibrated correction incompletely subtracting the Sr interferenceon the Zr line For the range of Sr abundances tested here this biasin Zr was always lt20 (relative)

Dry and wet sample powders were analyzed to assess matrix ef-fects arising from the presence of H2O A wet sample of JB-2 yieldedconcentrations that were on average ~20 lower compared tobracketing analyses from a dry JB-2 sample Packing standard pow-ders in the sample cups to different heights did not show any signif-icant differences for these elements but thick (to severalmillimeters) packing is critical for light elements Based on theseinitial tests samples were prepared as follows

1 Collect several grams of core sample 2 Freeze-dry sample for ~30 min 3 Grind sample to a fine powder using a corundum mortar or a

shatterbox for hard samples4 Transfer sample powder into the plastic sample cell and evenly

distribute it on the tightly seated polypropylene X-ray film held in place by a plastic ring

5 Cover sample powder with a 24 cm diameter filter paper6 Stuff the remaining space with polyester fiber to prevent sample

movement7 Close the sample cup with lid and attach sample label

Prior to analyzing unknowns a software-controlled system cali-bration was performed JB-2 (basalt from Izu-Oshima Volcano Ja-pan) was preferentially analyzed bracketing batches of 4ndash6unknowns to monitor instrument performance because its compo-sition is very similar to mafic tephra encountered during Expedition350 Data are reported as calculated in the factory-calibrated soilmode (except for Y which was calculated offline using a workingcurve from analysis of rock standards) regardless of potential sys-tematic deviations observed on the standards Results should onlybe considered as absolute abundances within the limits of the sys-tematic uncertainties constrained by the analysis of rock standardswhich are generally lt20 (Figure F13)

ICP-AESSample preparation

Selected samples of igneous and volcaniclastic rocks were ana-lyzed for major and trace element concentrations using ICP-AES

For unconsolidated volcaniclastic rock ash was sampled by scoop-ing whereas lapilli-sized juvenile clasts were hand-picked targetinga total sample volume of ~5 cm3 Consolidated (hard rock) igneousand volcaniclastic samples ranging in size from ~2 to ~8 cm3 werecut from the core with a diamond saw blade A thin section billetwas always taken from the same or adjacent interval to microscopi-cally check for alteration All cutting surfaces were ground on a dia-mond-impregnated disk to remove altered rinds and surfacecontamination derived from the drill bit or the saw Hard rockblocks were individually placed in a beaker containing trace-metal-grade methanol and washed ultrasonically for 15 min The metha-nol was decanted and the samples were washed in Barnstead DIwater (~18 MΩmiddotcm) for 10 min in an ultrasonic bath The cleanedpieces were dried for 10ndash12 h at 110degC

Figure F11 Working curve for shipboard pXRF analysis of Y Standardsinclude JB-2 JB-3 BHVO-2 BCR-2 AGV-1 JA-2 JR-1 JR-2 and JG-2 with Yabundances between 183 and 865 ppm Intensities of Y Kα were peak-stripped for Rb Kβ using the approach of Gaacutesquez et al (1997) All character-istic peak intensities were normalized to the Ag Compton intensity Count-ing errors are reported as 1σ

0 20 40 60 80 10000

01

02

03

04

Y K

α (n

orm

aliz

ed to

Ag

Com

pton

)

Y standard (ppm)

y = 000387 times x

Figure F12 Reproducibility of shipboard pXRF analysis of JB-2 powder overan ~7 week period in 2014 Errors are reported as 1σ equivalent to theobserved standard deviation

Oxi

de (

wt

)

Analysis date (mdd2014)

Ele

men

t (p

pm)

CaO = 953 plusmn 012 wt

K2O = 041 plusmn 001 wt

Sr = 170 plusmn 3 ppm

Zr = 52 plusmn 2 ppm

n = 131

Y = 24 plusmn 3 ppm

03

04

05

90

95

100

105

410 417 424 51 58 515 522 5290

20

40

60

150

170

190

Table T8 Values for standards measured by pXRF (averages) and true (refer-ences) values Download table in csv format



The cleaned dried samples were crushed to lt1 cm chips be-tween two disks of Delrin plastic in a hydraulic press Some samplescontaining obvious alteration were hand-picked under a binocularmicroscope to separate material as free of alteration phases as pos-sible The chips were then ground to a fine powder in a SPEX 8515shatterbox with a tungsten carbide lining After grinding an aliquotof the sample powder was weighed to 10000 plusmn 05 mg and ignited at700degC for 4 h to determine weight loss on ignition (LOI) Estimated

relative uncertainties for LOI determinations are ~14 on the basisof duplicate measurements

The ICP-AES analysis protocol follows the procedure in Murrayet al (2000) After determination of LOI 1000 plusmn 02 mg splits of theignited whole-rock powders were weighed and mixed with 4000 plusmn05 mg of LiBO2 flux that had been preweighed on shore Standardrock powders and full procedural blanks were included with un-knowns in each ICP-AES run (note that among the elements re-

Figure F13 Accuracy of shipboard pXRF analyses relative to international geochemical rock standards (solid circles Govindaraju 1994) and shipboard ICP-AESanalyses of samples collected and analyzed during Expedition 350

Ref

eren

ce

MnO (wt)Fe2O3 (wt)TiO2 (wt)

Standard

plusmn20 (rel)

000 005 010 015 020 025 030000

005

010

015

020

025

030

0 2 4 6 8 10 12 14 16 180

2

4

6

8

10

12

14

16

18

00 05 10 15 20 25 3000

05

10

15

20

25

30

Sr (ppm)

0 100 200 300 400 500 600 700 8000

100

200

300

400

500

600

700

800

CaO (wt)

0 2 4 6 8 10 12 140

2

4

6

8

10

12

14

Zn (ppm)

0 50 100 1500

50

100

150

Zr (ppm)

0 50 100 150 200 250 3000

50

100

150

200

250

300

K2O (wt)

0 1 2 3 4 500

05

10

15

20

25

30

35

40

45

50

Y (ppm)

0 10 20 30 40 50 60 700

10

20

30

40

50

60

70

pXRFICP-AES



ported contamination from the tungsten carbide mills is negligibleShipboard Scientific Party 2003) All samples and standards wereweighed on a Cahn C-31 microbalance (designed to measure at sea)with weighing errors estimated to be plusmn005 mg under relativelysmooth sea-surface conditions

To prevent the cooled bead from sticking to the crucible 10 mLof 0172 mM aqueous LiBr solution was added to the mixture of fluxand rock powder as a nonwetting agent Samples were then fusedindividually in Pt-Au (955) crucibles for ~12 min at a maximumtemperature of 1050degC in an internally rotating induction furnace(Bead Sampler NT-2100)

After cooling beads were transferred to high-density polypro-pylene bottles and dissolved in 50 mL of 10 (by volume) HNO3aided by shaking with a Burrell wrist-action bottle shaker for 1 hFollowing digestion of the bead the solution was passed through a045 μm filter into a clean 60 mL wide-mouth high-density polypro-pylene bottle Next 25 mL of this solution was transferred to a plas-tic vial and diluted with 175 mL of 10 HNO3 to bring the totalvolume to 20 mL The final solution-to-sample dilution factor was~4000 For standards stock standard solutions were placed in an ul-trasonic bath for 1 h prior to final dilution to ensure a homogeneoussolution

Analysis and data reductionMajor (Si Ti Al Fe Mn Mg Ca Na K and P) and trace (Sc V

Cr Co Ni Cu Zn Rb Sr Y Zr Nb Ba and Th) element concentra-tions of standards and samples were analyzed with a Teledyne Lee-man Labs Prodigy ICP-AES instrument (Table T7) For severalelements measurements were performed at more than one wave-length (eg Si at 250690 and 251611 nm) and data with the leastscatter and smallest deviations from the check standard values wereselected

The plasma was ignited at least 30 min before each run of sam-ples to allow the instrument to warm up and stabilize A zero-ordersearch was then performed to check the mechanical zero of the dif-fraction grating After the zero-order search the mechanical steppositions of emission lines were tuned by automatically searchingwith a 0002 nm window across each emission peak using single-el-ement solutions

The ICP-AES data presented in the Geochemistry section ofeach site chapter were acquired using the Gaussian mode of the in-strument software This mode fits a curve to points across a peakand integrates the area under the curve for each element measuredEach sample was analyzed four times from the same dilute solution(ie in quadruplicate) within a given sample run For elements mea-sured at more than one wavelength we either used the wavelengthgiving the best calibration line in a given run or if the calibrationlines for more than one wavelength were of similar quality used thedata for each and reported the average concentration

A typical ICP-AES run (Table T9) included a set of 9 or 10 certi-fied rock standards (JP-1 JB-2 AGV STM-1 GSP-2 JR-1 JR-2BHVO-2 BCR-2 and JG-3) analyzed together with the unknownsin quadruplicate A 10 HNO3 wash solution was introduced for 90s between each analysis and a solution for drift correction was ana-lyzed interspersed with the unknowns and at the beginning and endof each run Blank solutions aspirated during each run were belowdetection for the elements reported here JB-2 was also analyzed asan unknown because it is from the Bonin arc and its compositionmatches closely the Expedition 350 unknowns (Table T10)

Measured raw intensities were corrected offline for instrumentdrift using the shipboard ICP Analyzer software A linear calibra-

tion line for each element was calculated using the results for thecertified rock standards Element concentrations in the sampleswere then calculated from the relevant calibration lines Data wererejected if total volatile-free major element weight percentages to-tals were outside 100 plusmn 5 wt Sources of error include weighing(particularly in rougher seas) sample and standard dilution and in-strumental instabilities To facilitate comparison of Expedition 350results with each other and with data from the literature major ele-ment data are reported normalized to 100 wt total Total iron isstated as total FeO or Fe2O3 Precision and accuracy based on rep-licate analyses of JB-2 range between ~1 and 2 (relative) for ma-jor oxides and between ~1 and 13 (relative) for minor and tracecomponents (Table T10)

Physical propertiesShipboard physical properties measurements were undertaken

to provide a general and systematic characterization of the recov-ered core material detect trends and features related to the devel-opment and alteration of the formations and infer causal processesand depositional settings Physical properties are also used to linkgeological observations made on the core to downhole logging dataand regional geophysical survey results The measurement programincluded the use of several core logging and discrete sample mea-surement systems designed and built at IODP (College StationTexas) for specific shipboard workflow requirements

After cores were cut into 15 m (or shorter) sections and hadwarmed to ambient laboratory temperature (~20degC) all core sec-tions were run through two core logger systems the WRMSL andthe NGRL The WRMSL includes a gamma ray attenuation (GRA)bulk densitometer a magnetic susceptibility logger (MSL) and a P-wave logger (PWL) Thermal conductivity measurements were car-ried out using the needle probe technique if the material was softenough For lithified sediment and rocks thermal conductivity wasmeasured on split cores using the half-space technique

After the sections were split into working and archive halves thearchive half was processed through the SHIL to acquire high-reso-lution images of split core followed by the SHMSL for color reflec-tance and point magnetic susceptibility (MSP) measurements witha contact probe The working half was placed on the Section HalfMeasurement Gantry (SHMG) where P-wave velocity was mea-sured using a P-wave caliper (PWC) and if the material was softenough a P-wave bayonet (PWB) each equipped with a pulser-re-ceiver system P-wave measurements on section halves are often ofsuperior quality to those on whole-round sections because of bettercoupling between the sensors and the sediment PWL measure-ments on the whole-round logger have the advantage of being ofmuch higher spatial resolution than those produced by the PWCShear strength was measured using the automated vane shear (AVS)apparatus where the recovered material was soft enough

Discrete samples were collected from the working halves formoisture and density (MAD) analysis

The following sections describe the measurement methods andsystems in more detail A full discussion of all methodologies and

Table T9 Selected sequence of analyses in ICP-AES run Expedition 350Download table in csv format

Table T10 JB-2 check standard major and trace element data for ICP-AESanalysis Expedition 350 Download table in csv format



calculations used aboard the JOIDES Resolution in the PhysicalProperties Laboratory is available in Blum (1997)

Gamma ray attenuation bulk densitySediment bulk density can be directly derived from the mea-

surement of GRA (Evans 1965) The GRA densitometer on theWRMSL operates by passing gamma radiation from a Cesium-137source through a whole-round section into a 75 mm sodium iodidedetector situated vertically under the source and core section Thegamma ray (principal energy = 662 keV) is attenuated by Comptonscattering as it passes through the core section The attenuation is afunction of the electron density and electron density is related tothe bulk density via the mass attenuation coefficient For the major-ity of elements and for anhydrous rock-forming minerals the massattenuation coefficient is ~048 whereas for hydrogen it is 099 Fora two-phase system including minerals and water and a constant ab-sorber thickness (the core diameter) the gamma ray count is pro-portional to the mixing ratio of solids with water and thus the bulkdensity

The spatial resolution of the GRA densitometer measurementsis lt1 cm The quality of GRA data is highly dependent on the struc-tural integrity of the core because of the high resolution (ie themeasurements are significantly affected by cracks voids and re-molded sediment) The absolute values will be lower if the sedimentdoes not completely fill the core liner (ie if gas seawater or slurryfill the gap between the sediment and the core liner)

GRA precision is proportional to the square root of the countsmeasured as gamma ray emission is subject to Poisson statisticsCurrently GRA measurements have typical count rates of 10000(dense rock) to 20000 countss (soft mud) If measured for 4 s thestatistical error of a single measurement is ~05 Calibration of thedensitometer was performed using a core liner filled with distilledwater and aluminum segments of variable thickness Recalibrationwas performed if the measured density of the freshwater standarddeviated by plusmn002 gcm3 (2) GRA density was measured at the in-terval set on the WRMSL for the entire expedition (ie 5 cm)

Magnetic susceptibilityLow-field magnetic susceptibility (MS) is the degree to which a

material can be magnetized in an external low-magnetization (le05mT) field Magnetic susceptibility of rocks varies in response to themagnetic properties of their constituents making it useful for theidentification of mineralogical variations Materials such as claygenerally have a magnetic susceptibility several orders of magnitudelower than magnetite and some other iron oxides that are commonconstituents of igneous material Water and plastics (core liner)have a slightly negative magnetic susceptibility

On the WRMSL volume magnetic susceptibility was measuredusing a Bartington Instruments MS2 meter coupled to a MS2C sen-sor coil with a 90 mm diameter operating at a frequency of 0565kHz We refer to these measurements as MSL MSL was measuredat the interval set on the WRMSL for the entire expedition (ie 5cm)

On the SHMSL volume magnetic susceptibility was measuredusing a Bartington Instruments MS2K meter and contact probewhich is a high-resolution surface scanning sensor with an operat-ing frequency of 093 kHz The sensor has a 25 mm diameter re-sponse pattern (full width and half maximum) The responsereduction is ~50 at 3 mm depth and 10 at 8 mm depth We refer

to these as MSP measurements Because the MS2K demands flushcontact between the probe and the section-half surface the archivehalves were covered with clear plastic wrap to avoid contaminationMeasurements were generally taken at 25 cm intervals the intervalwas decreased to 1 cm when time permitted

Magnetic susceptibility from both instruments is reported in in-strument units To obtain results in dimensionless SI units the in-strument units need to be multiplied by a geometric correctionfactor that is a function of the probe type core diameter and loopsize Because we are not measuring the core diameter application ofa correction factor has no benefit over reporting instrument units

P-wave velocityP-wave velocity is the distance traveled by a compressional P-

wave through a medium per unit of time expressed in meters persecond P-wave velocity is dependent on the composition mechan-ical properties porosity bulk density fabric and temperature of thematerial which in turn are functions of consolidation and lithifica-tion state of stress and degree of fracturing Occurrence and abun-dance of free gas in soft sediment reduces or completely attenuatesP-wave velocity whereas gas hydrates may increase P-wave velocityP-wave velocity along with bulk density data can be used to calcu-late acoustic impedances and reflection coefficients which areneeded to construct synthetic seismic profiles and estimate thedepth of specific seismic horizons

Three instrument systems described here were used to measureP-wave velocity

The PWL system on the WRMSL transmits a 500 kHz P-wavepulse across the core liner at a specified repetition rate The pulserand receiver are mounted on a caliper-type device and are aligned inorder to make wave propagation perpendicular to the sectionrsquos longaxis A linear variable differential transducer measures the P-wavetravel distance between the pulse source and the receiver Goodcoupling between transducers and core liner is facilitated with wa-ter dripping onto the contact from a peristaltic water pump systemSignal processing software picks the first arrival of the wave at thereceiver and the processing routine also corrects for the thicknessof the liner As for all measurements with the WRMSL the mea-surement intervals were 5 cm

The PWC system on the SHMG also uses a caliper-type config-uration for the pulser and receiver The system uses Panametrics-NDT Microscan delay line transducers which transmit an ultra-sonic pulse at 500 kHz The distance between transducers is mea-sured with a built-in linear voltage displacement transformer Onemeasurement was in general performed on each section with ex-ceptions as warranted

A series of acrylic cylinders of varying thicknesses are used tocalibrate both the PWL and the PWC systems The regression oftraveltime versus travel distance yields the P-wave velocity of thestandard material which should be within 2750 plusmn 20 ms Thethickness of the samples corrected for liner thickness is divided bythe traveltime to calculate P-wave velocity in meters per second Onthe PWL system the calibration is verified by measuring a core linerfilled with pure water and the calibration passes if the measured ve-locity is within plusmn20 ms of the expected value for water at roomtemperature (1485 ms) On the PWC system the calibration is ver-ified by measuring the acrylic material used for calibration

The PWB system on the SHMG uses transducers built into bay-onet-style blades that can be inserted into soft sediment The dis-



tance between the pulser and receiver is fixed and the traveltime ismeasured Calibration is performed with a split liner half filled withpure water using a known velocity of 1485 ms at 22degC

On both the PWC and the PWB systems the user has the optionto override the automated pulse arrival particularly in the case of aweak signal and pick the first arrival manually

Natural gamma radiationNatural gamma radiation (NGR) is emitted from Earth materials

as a result of the radioactive decay of 238U 232Th and 40K isotopesMeasurement of NGR from the recovered core provides an indica-tion of the concentration of these elements and can be compareddirectly against downhole NGR logs for core-log integration

NGR was measured using the NGRL The main NGR detectorunit consists of 8 sodium iodide (NaI) scintillation detectors spacedat ~20 cm intervals along the core axis 7 active shield plastic scintil-lation detectors 22 photomultipliers and passive lead shielding(Vasiliev et al 2011)

A single measurement run with the NGRL provides 8 measure-ments at 20 cm intervals over a 150 cm section of core To achieve a10 cm measurement interval the NGRL automatically records twosets of measurements offset by 10 cm The quality of the energyspectrum measured depends on the concentration of radionuclidesin the sample and on the counting time A live counting time of 5min was set in each position (total live count time of 10 min per sec-tion)

Thermal conductivityThermal conductivity (k in W[mmiddotK]) is the rate at which heat is

conducted through a material At steady state thermal conductivityis the coefficient of heat transfer (q) across a steady-state tempera-ture (T) difference over a distance (x)

q = k(dTdx)

Thermal conductivity of Earth materials depends on many fac-tors At high porosities such as those typically encountered in softsediment porosity (or bulk density water content) the type of satu-rating fluid and temperature are the most important factors affect-ing thermal conductivity For low-porosity materials compositionand texture of the mineral phases are more important

A TeKa TK04 system measures and records the changes in tem-perature with time after an initial heating pulse emitted from asuperconductive probe A needle probe inserted into a small holedrilled through the plastic core liner is used for soft-sediment sec-tions whereas hard rock samples are measured by positioning a flatneedle probe embedded into a plastic puck holder onto the flat sur-faces of split core pieces The TK04 system measures thermal con-ductivity by transient heating of the sample with a known heatingpower and geometry Changes in temperature with time duringheating are recorded and used to calculate thermal conductivityHeating power can be adjusted for each sample as a rule of thumbheating power (Wm) is set to be ~2 times the expected thermalconductivity (ie ~12ndash2 W[mmiddotK]) The temperature of the super-conductive probe has a quasilinear relationship with the natural log-arithm of the time after heating initiation The TK04 device uses aspecial approximation method to calculate conductivity and to as-sess the fit of the heating curve This method fits discrete windowsof the heating curve to the theoretical temperature (T) with time (t)function

T(t) = A1 + A2 ln(t) + A3 [ln(t)t] + (A4t)

where A1ndashA4 are constants that are calculated by linear regressionA1 is the initial temperature whereas A2 A3 and A4 are related togeometry and material properties surrounding the needle probeHaving defined these constants (and how well they fit the data) theapparent conductivity (ka) for the fitted curve is time dependent andgiven by

ka(t) = q4πA2 + A3[1 minus ln(t)t] minus (A4t)

where q is the input heat flux The maximum value of ka and thetime (tmax) at which it occurs on the fitted curve are used to assessthe validity of that time window for calculating thermal conductiv-ity The best solutions are those where tmax is greatest and thesesolutions are selected for output Fits are considered good if ka has amaximum value tmax is large and the standard deviation of theleast-squares fit is low For each heating cycle several output valuescan be used to assess the quality of the data including natural loga-rithm of extreme time tmax which should be large the number ofsolutions (N) which should also be large and the contact valuewhich assesses contact resistance between the probe and the sampleand should be small and uniform for repeat measurements

Thermal conductivity values can be multiplied with downholetemperature gradients at corresponding depths to produce esti-mates of heat flow in the formation (see Downhole measure-ments)

Moisture and densityIn soft to moderately indurated sediments working section

halves were sampled for MAD analysis using plastic syringes with adiameter only slightly less than the diameter of the preweighed 16mL Wheaton glass vials used to process and store the samples of~10 cm3 volume Typically 1 sample per section was collectedSamples were taken at irregular intervals depending on the avail-ability of material homogeneous and continuous enough for mea-surement

In indurated sediments and rocks cubes of ~8 cm3 were cutfrom working halves and were saturated with a vacuum pump sys-tem The system consists of a plastic chamber filled with seawater Avacuum pump then removes air from the chamber essentially suck-ing air from pore spaces Samples were kept under vacuum for atleast 24 h During this time pressure in the chamber was monitoredperiodically by a gauge attached to the vacuum pump to ensure astable vacuum After removal from the saturator cubes were storedin sample containers filled with seawater to maintain saturation

The mass of wet samples was determined to a precision of 0005g using two Mettler-Toledo electronic balances and a computer av-eraging system to compensate for the shiprsquos motion The sampleswere then heated in an oven at 105deg plusmn 5degC for 24 h and allowed tocool in a desiccator for 1 h The mass of the dry sample was deter-mined with the same balance system Dry sample volume was deter-mined using a 6-celled custom-configured Micromeritics AccuPyc1330TC helium-displacement pycnometer system The precision ofeach cell volume is 1 of the full-scale volume Volume measure-ment was preceded by three purges of the sample chamber with he-lium warmed to ~28degC Three measurement cycles were run foreach sample A reference volume (calibration sphere) was placed se-quentially in one of the six chambers to check for instrument driftand systematic error The volumes of the numbered Wheaton vials



were calculated before the cruise by multiplying each vialrsquos massagainst the average density of the vial glass

The procedures for the determination of the MAD phase rela-tionships comply with the American Society for Testing and Materi-als (ASTM International 1990) and are discussed in detail by Blum(1997) The method applicable to saturated fine-grained sedimentsis called ldquoMethod Crdquo Method C is based on the measurement of wetmass dry mass and volume It is not reliable or adapted for uncon-solidated coarse-grained sediments in which water can be easily lostduring the sampling (eg in foraminifer sands often found at thetop of the hole)

Wet mass (Mwet) dry mass (Mdry) and dry volume (Vdry) weremeasured in the laboratory Wet bulk density (ρwet) dry bulk density(ρdry) sediment grain density (ρsolid) porosity (φ) and void ratio(VR) were calculated as follows

ρwet = MwetVwet

ρdry = MsolidVwet

ρsolid = MsolidVsolid

φ = VpwVwet

and

VR = VpwVsolid

where the volume of pore water (Vpw) mass of solids excluding salt(Msolid) volume of solids excluding salt (Vsolid) and wet volume(Vwet) were calculated using the following parameters (Blum 1997ASTM International 1990)

Mass ratio (rm) = 0965 (ie 0965 g of freshwater per 1 g of sea-water)

Salinity (s) = 0035Pore water density (ρpw) = 1024 gcm3Salt density (ρsalt) = 222 gcm3

An accuracy and precision of MAD measurements of ~05 canbe achieved with the shipboard devices The largest source of poten-tial error is the loss of material or moisture during the ~30ndash48 hlong procedure for each sample

Sediment strengthShear strength of soft sedimentary samples was measured using

the AVS by Giesa The Giesa system consists of a controller and agantry for shear vane insertion A four-bladed miniature vane (di-ameter = height = 127 mm) was pushed carefully into the sedimentof the working halves until the top of the vane was level with thesediment surface The vane was then rotated at a constant rate of90degmin to determine the torque required to cause a cylindrical sur-face to be sheared by the vane This destructive measurement wasdone with the rotation axis parallel to the bedding plane The torquerequired to shear the sediment along the vertical and horizontaledges of the vane is a relatively direct measurement of shearstrength Undrained shear strength (su) is given as a function ofpressure in SI units of pascals (kPa = kNm2)

Strength tests were performed on working halves from APCcores at a resolution of 1 measurement per section

Color reflectanceReflectance of ultraviolet to near-infrared light (171ndash1100 nm

wavelength at 2 nm intervals) was measured on archive half surfacesusing an Ocean Optics USB4000 spectrophotometer mounted onthe SHMSL Spectral data are routinely reduced to the Lab colorspace parameters for output and presentation in which L is lumi-nescence a is the greenndashred value and b is the bluendashyellow valueThe color reflectance spectrometer calibrates on two spectra purewhite (reference) and pure black (dark) Measurements were takenat 25 cm intervals and rarely at 1 cm intervals

Because the reflectance integration sphere requires flush con-tact with the section-half surface the archive halves were coveredwith clear plastic wrap to avoid contamination The plastic filmadds ~1ndash5 error to the measurements Spurious measurementswith larger errors can result from small cracks or sediment distur-bance caused by the drilling process

PaleomagnetismSamples instruments and measurementsPaleomagnetic studies during Expedition 350 principally fo-

cused on measuring the natural remanent magnetization (NRM) ofarchive section halves on the superconducting rock magnetometer(SRM) before and after alternating field (AF) demagnetization Ouraim was to produce a magnetostratigraphy to merge with paleonto-logical datums to yield the age model for each of the two sites (seeAge model) Analysis of the archive halves was complemented bystepwise demagnetization and measurement of discrete cube speci-mens taken from the working half these samples were demagne-tized to higher AF levels and at closer AF intervals than was the casefor sections measured on the SRM Some discrete samples werethermally demagnetized

Demagnetization was conducted with the aim of removing mag-netic overprints These arise both naturally particularly by the ac-quisition of viscous remanent magnetization (VRM) and as a resultof drilling coring and sample preparation Intense usually steeplyinclined overprinting has been routinely described from ODP andIntegrated Ocean Drilling Program cores and results from exposureof the cores to strong magnetic fields because of magnetization ofthe core barrel and elements of the BHA and drill string (Stokking etal 1993 Richter et al 2007) The use of nonmagnetic stainless steelcore barrels during APC coring during Expedition 350 reduced theseverity of this drilling-induced overprint (Lund et al 2003)

Discrete cube samples for paleomagnetic analysis were collectedboth when the core sections were relatively continuous and undis-turbed (usually the case in APC-cored intervals) and where discon-tinuous recovery or core disturbance made use of continuoussections unreliable (in which case the discrete samples became thesole basis for magnetostratigraphy) We collected one discrete sam-ple per section through all cores at both sites A subset of these sam-ples after completion of stepwise AF demagnetization andmeasurement of the demagnetized NRM were subjected to furtherrock-magnetic analysis These analyses comprised partial anhyster-etic remanent magnetization (pARM) acquisition and isothermalremanent magnetization (IRM) acquisition and demagnetizationwhich helped us to assess the nature of magnetic carriers and thedegree to which these may have been affected by postdepositionalprocesses both during early diagenesis and later alteration This al-lowed us to investigate the lock-in depth (the depth below seafloor



at which postdepositional processes ceased to alter the NRM) andto adjust AF demagnetization levels to appropriately isolate the de-positional (or early postdepositional) characteristic remanent mag-netization (ChRM) We also examined the downhole variation inrock-magnetic parameters as a proxy for alteration processes andcompared them with the physical properties and lithologic profiles

Archive section half measurementsMeasurements of remanence and stepwise AF demagnetization

were conducted on archive section halves with the SRM drivenwith the SRM software (Version 318) The SRM is a 2G EnterprisesModel 760R equipped with direct-current superconducting quan-tum interference devices and an in-line automated 3-axis AF de-magnetizer capable of reaching a peak field of 80 mT The spatialresolution measured by the width at half-height of the pick-up coilsresponse is lt10 cm for all three axes although they sense a magne-tization over a core length up to 30 cm The magnetic momentnoise level of the cryogenic magnetometer is ~2 times 10minus10 Am2 Thepractical noise level however is affected by the magnetization ofthe core liner and the background magnetization of the measure-ment tray resulting in a lower limit of magnetization of ~2 times 10minus5

Am that can be reliably measuredWe measured the archive halves at 25 cm intervals and they

were passed through the sensor at a speed of 10 cms Two addi-tional 15 cm long intervals in front of and behind the core sectionrespectively were also measured These header and trailer measure-ments serve the dual functions of monitoring background magneticmoment and allowing for future deconvolution analysis After aninitial measurement of undemagnetized NRM we proceeded to de-magnetize the archive halves over a series of 10 mT steps from 10 to40 mT We chose the upper demagnetization limit to avoid contam-ination by a machine-induced anhysteretic remanent magnetization(ARM) which was reported during some previous IntegratedOcean Drilling Program expeditions (Expedition 324 Scientists2010) In some cores we found that the final (40 mT) step did notimprove the definition of the magnetic polarity so to improve therate of core flow through the lab we discontinued the 40 mT demag-netization step in these intervals NRM after AF demagnetizationwas plotted for individual sample points as vector plots (Zijderveld1967) to assess the effectiveness of overprint removal as well asplots showing variations with depth at individual demagnetizationlevels We inspected the plots visually to judge whether the rema-nence after demagnetization at the highest AF step reflected theChRM and geomagnetic polarity sequence

Discrete samplesWhere the sediment was sufficiently soft we collected discrete

samples in plastic ldquoJapaneserdquo Natsuhara-Giken sampling boxes(with a sample volume of 7 cm3) In soft sediment these boxes werepushed into the working half of the core by hand with the up arrowon the box pointing upsection in the core As the sediment becamestiffer we extracted samples from the section with a stainless steelsample extruder we then extruded the sample onto a clean plateand carefully placed a Japanese box over it Note that this methodretained the same orientation relative to the split core face of push-in samples In more indurated sediment we cut cubes with orthog-onal passes of a tile saw with 2 parallel blades spaced 2 cm apartWhere the resulting samples were friable we fitted the resultingsample into an ldquoODPrdquo plastic cube For lithified intervals we simply

marked an upcore orientation arrow on the split core face of the cutcube sample These lithified samples without a plastic liner wereavailable for both AF and thermal demagnetization

Remanence measurementsWe measured the NRM of discrete samples before and after de-

magnetization on an Agico JR-6A dual-speed spinner magnetome-ter (sensitivity = ~2 times 10minus6 Am) We used the automatic sampleholder for measuring the Japanese cubes and lithified cubes withouta plastic liner For semilithified samples in ODP plastic cubes whichare too large to fit the automatic holder we used the manual holderin 4 positions Although we initially used high-speed rotation wefound that this resulted in destruction of many fragile samples andin slippage and rotation failure in many of the Japanese boxes so wechanged to slow rotation speed until we again encountered suffi-ciently lithified samples Progressive AF demagnetization of the dis-crete samples was achieved with a DTech D-2000 AF demagnetizerat 5 mT intervals from 5 to 50 mT followed by steps at 60 80 and100 mT Most samples were not demagnetized through the fullnumber of steps rather routine demagnetization for determiningmagnetic polarity was carried out only until the sign of the mag-netic inclination was clearly defined (15ndash20 mT in most samples)Some selected samples were demagnetized to higher levels to testthe efficiency of the demagnetization scheme

We thermally demagnetized a subset of the lithified cube sam-ples as an alternative more effective method of demagnetizinghigh-coercivity materials (eg hematite) that is also efficient at re-moving the magnetization of magnetic sulfides particularly greig-ite which thermally decomposes during heating in air attemperatures of 300degndash400degC (Roberts and Turner 1993 Musgraveet al 1995) Difficulties in thermally demagnetizing samples inplastic boxes discouraged us from applying this method to softersamples We demagnetized these samples in a Schonstedt TSD-1thermal demagnetizer at 50degC temperature steps from 100deg to 400degCand then 25degC steps up to a maximum of 600degC and measured de-magnetized NRM after each step on the spinner magnetometer Aswith AF demagnetization we limited routine thermal demagnetiza-tion to the point where only a single component appeared to remainand magnetic inclination was clearly established A subset of sam-ples was continued through the entire demagnetization programBecause thermal demagnetization can lead to generation of newmagnetic minerals capable of acquiring spurious magnetizationswe monitored such alteration by routine measurements of the mag-netic susceptibility following remanence measurement after eachthermal demagnetization step We measured magnetic susceptibil-ity of discrete samples with a Bartington MS2 susceptibility meterusing an MS2C loop sensor

Sample sharing with physical propertiesIn order to expedite sample flow at Site U1437 some paleomag-

netic analysis was conducted on physical properties samples alreadysubjected to MAD measurement MAD processing involves watersaturation of the samples followed by drying at 105degC for 24 h in anenvironment exposed to the ambient magnetic field Consequentlythese samples acquired a laboratory-induced overprint which wetermed the ldquoMAD overprintrdquo We measured the remanence of thesesamples after they returned from the physical properties team andagain after thermal demagnetization at 110degC before continuingwith further AF or thermal demagnetization



Liquid nitrogen treatmentMultidomain magnetite with grain sizes typically greater than

~1 μm does not exhibit the simple relationship between acquisitionand unblocking temperatures predicted by Neacuteel (1949) for single-domain grains low-temperature overprints carried by multidomaingrains may require very high demagnetization temperatures to re-move and in fact it may prove impossible to isolate the ChRMthrough thermal demagnetization Similar considerations apply toAF demagnetization For this reason when we had evidence thatoverprints in multidomain grains were obscuring the magneto-stratigraphic signal we instituted a program of liquid nitrogen cool-ing of the discrete samples in field-free space (see Dunlop et al1997) This comprised inserting the samples (after first drying themduring thermal demagnetization at 110degndash150degC) into a bath of liq-uid nitrogen held in a Styrofoam container which was then placedin a triple-layer mu-metal cylindrical can to provide a (near) zero-field environment We allowed the nitrogen to boil off and the sam-ples to warm Cooling of the samples to the boiling point of nitrogen(minus196degC) forces the magnetite to acquire a temperature below theVerwey transition (Walz 2002) at about minus153degC Warming withinfield-free space above the transition allows remanence to recover insingle-domain grains but randomizes remanence in multidomaingrains (Dunlop 2003) Once at room temperature the samples weretransferred to a smaller mu-metal can until measurement to avoidacquisition of VRM The remanence of these samples was mea-sured and then routine thermal or AF demagnetization continued

Rock-magnetic analysisAfter completion of AF demagnetization we selected two sub-

sets of discrete samples for rock-magnetic analysis to identify mag-netic carriers by their distribution of coercivity High-coercivityantiferromagnetic minerals (eg hematite) which magnetically sat-urate at fields in excess of 300 mT can be distinguished from ferro-magnetic minerals (eg magnetite) by the imposition of IRM Onthe first subset of discrete samples we used an ASC Scientific IM-10 impulse magnetometer to impose an IRM in a field of 1 T in the+z (downcore)-direction and we measured the IRM (IRM1T) withthe spinner magnetometer We subsequently imposed a secondIRM at 300 mT in the opposite minusz-direction and measured the re-sultant IRM (ldquobackfield IRMrdquo [IRMminus03T]) The ratio Sminus03T =[(IRMminus03TIRM1T) + 1]2 is a measure of the relative contribution ofthe ferrimagnetic and antiferromagnetic populations to the totalmagnetic mineralogy (Bloemendal et al 1992)

We subjected the second subset of discrete samples to acquisi-tion of pARM over a series of coercivity intervals using the pARMcapability of the DTech AF demagnetizer This technique which in-volves applying a bias field during part of the AF demagnetizationcycle when the demagnetizing field is decreasing allows recogni-tion of different coercivity spectra in the ferromagnetic mineralogycorresponding to different sizes or shapes of grains (eg Jackson etal 1988) or differing mineralogy or chemistry (eg varying Ti sub-stitution in titanomagnetite) We imparted pARM using a 01 mTbias field aligned along the +z-axis and a peak demagnetization fieldof 100 mT over a series of 10 mT coercivity windows up to 100 mT

Anisotropy of magnetic susceptibilityAt Site U1437 we carried out magnetic fabric analysis in the

form of anisotropy of magnetic susceptibility (AMS) measure-ments both as a measure of sediment compaction and to determinethe compaction correction needed to determine paleolatitudesfrom magnetic inclination We carried this out on a subset of dis-crete samples using an Agico KLY 4 magnetic susceptibility meter

We calculated anisotropy as the foliation (F) = K2K3 and the linea-tion (L) = K1K2 where K1 K2 and K3 are the maximum intermedi-ate and minimum eigenvalues of the anisotropy tensor respectively

Sample coordinatesAll magnetic data are reported relative to IODP orientation con-

ventions +x is into the face of the working half +y points towardthe right side of the face of the working half (facing upsection) and+z points downsection The relationship of the SRM coordinates(x‑ y- and z-axes) to the data coordinates (x- y- and z-directions)is as follows for archive halves x-direction = x-axis y-direction =minusy-axis and z-direction = z-axis for working halves x-direction =minusx-axis y-direction = y-axis and z-direction = z-axis (Figure F14)Discrete cubes are marked with an arrow on the split face (or thecorresponding face of the plastic box) in the upsection (ie minusz-di-rection)

Core orientationWith the exception of the first two or three APC cores (where

the BHA is not stabilized in the surrounding sediment) full-lengthAPC cores taken during Expedition 350 were oriented by means ofthe FlexIT orientation tool The FlexIT tool comprises three mutu-ally perpendicular fluxgate magnetic sensors and two perpendiculargravity sensors allowing the azimuth (and plunge) of the fiduciallines on the core barrel to be determined Nonmagnetic (Monel)APC barrels and a nonmagnetic drill collar were used during APCcoring (with the exception of Holes U1436B U1436C and U1436D)to allow accurate registration against magnetic north

MagnetostratigraphyExpedition 350 drill sites are located at ~32degN a sufficiently high

latitude to allow magnetostratigraphy to be readily identified bychanges in inclination alone By considering the mean state of theEarthrsquos magnetic field to be a geocentric axial dipole it is possible to

Figure F14 A Paleomagnetic sample coordinate systems B SRM coordinatesystem on the JOIDES Resolution (after Harris et al 2013)

Working half

+x = north+y = east

Bottom

+z

+y

+xTop

Top

Upcore

Upcore

Bottom

+x+z

+y

Archive half

270deg

0deg

90deg

180deg

90deg270deg

N

E

S

W

Double line alongaxis of core liner

Single line along axis of core liner

Discrete sample

Up

Bottom Up arrow+z+y

+x

Japanese cube

Pass-through magnetometer coordinate system

A

B+z

+y

+x

+x +z

+y+z

+y

+x

Top Archive halfcoordinate system

Working halfcoordinate system



calculate the field inclination (I) by tan I = 2tan(lat) where lat is thelatitude Therefore the time-averaged normal field at the present-day positions of Sites U1436 and U1437 has a positive (downward)inclination of 5176deg and 5111deg respectively Negative inclinationsindicate reversed polarity Magnetozones identified from the ship-board data were correlated to the geomagnetic polarity timescale

(GPTS) (GPTS2012 Gradstein et al 2012) with the aid of biostrati-graphic datums (Table T11) In this updated GPTS version the LateCretaceous through Neogene time has been calibrated with magne-tostratigraphic biostratigraphic and cyclostratigraphic studies andselected radioisotopically dated datums The chron terminology isfrom Cande and Kent (1995)

Table T11 Age estimates for timescale of magnetostratigraphic chrons T = top B = bottom Note that Chron C14 does not exist (Continued on next page)Download table in csv format

Chron Datum Age Name

C1n B 0781 BrunhesMatuyamaC1r1n T 0988 Jaramillo top

B 1072 Jaramillo baseC2n T 1778 Olduvai top

B 1945 Olduvai baseC2An1n T 2581 MatuyamaGauss

B 3032 Kaena topC2An2n T 3116 Kaena base

B 3207 Mammoth topC2An3n T 3330 Mammoth base

B 3596 GaussGilbertC3n1n T 4187 Cochiti top

B 4300 Cochiti baseC3n2n T 4493 Nunivak top

B 4631 Nunivak baseC3n3n T 4799 Sidufjall top

B 4896 Sidufjall baseC3n4n T 4997 Thvera top

B 5235 Thvera baseC3An1n T 6033 Gilbert base

B 6252C3An2n T 6436

B 6733C3Bn T 7140

B 7212C3Br1n T 7251

B 7285C3Br2n T 7454

B 7489C4n1n T 7528

B 7642C4n2n T 7695

B 8108C4r1n T 8254

B 8300C4An T 8771

B 9105C4Ar1n T 9311

B 9426C4Ar2n T 9647

B 9721C5n1n T 9786

B 9937C5n2n T 9984

B 11056C5r1n T 11146

B 11188C5r2r-1n T 11263

B 11308C5r2n T 11592

B 11657C5An1n T 12049

B 12174C5An2n T 12272

B 12474C5Ar1n T 12735

B 12770C5Ar2n T 12829

B 12887C5AAn T 13032

B 13183

C5ABn T 13363B 13608

C5ACn T 13739B 14070

C5ADn T 14163B 14609

C5Bn1n T 14775B 14870

C5Bn2n T 15032B 15160

C5Cn1n T 15974B 16268

C4Cn2n T 16303B 16472

C5Cn3n T 16543B 16721

C5Dn T 17235B 17533

C5Dr1n T 17717B 17740

C5En T 18056B 18524

C6n T 18748B 19722

C6An1n T 20040B 20213

C6An2n T 20439B 20709

C6AAn T 21083B 21159

C6AAr1n T 21403B 21483

C6AAr2n T 21659B 21688

C6Bn1n T 21767B 21936

C6Bn1n T 21992B 22268

C6Cn1n T 22564B 22754

C6Cn2n T 22902B 23030

C6Cn3n T 23233B 23295

C7n1n T 23962B 24000

C7n2n T 24109B 24474

C7An T 24761B 24984

C81n T 25099B 25264

C82n T 25304B 25987

C9n T 26420B 27439

C10n1n T 27859B 28087

C10n2n T 28141B 28278

C11n1n T 29183




B 29477C11n2n T 29527

B 29970C12n T 30591

B 31034C13n T 33157

B 33705C15n T 34999

B 35294C16n1n T 35706

B 35892C16n2n T 36051

B 36700C17n1n T 36969

B 37753C17n2n T 37872

B 38093C17n3n T 38159

B 38333C18n1n T 38615

B 39627C18n2n T 39698

B 40145C19n T 41154

B 41390C20n T 42301

B 43432C21n T 45724

B 47349C22n T 48566

B 49344C23n1n T 50628

B 50835C23n2n T 50961

B 51833C24n1n T 52620

B 53074C24n2n T 53199

B 53274C24n3n T 53416

B 53983


Table T11 (continued)

BiostratigraphyPaleontology and biostratigraphy

Paleontological investigations carried out during Expedition350 focused on calcareous nannofossils and planktonic and benthicforaminifers Preliminary biostratigraphic determinations werebased on nannofossils and planktonic foraminifers Biostratigraphicinterpretations of planktonic foraminifers and biozones are basedon Wade et al (2011) with the exception of the bioevents associatedwith Globigerinoides ruber for which we refer to Li (1997) Benthicforaminifer species determination was mostly carried out with ref-erence to ODP Leg 126 records by Kaiho (1992) The standard nan-nofossil zonations of Martini (1971) and Okada and Bukry (1980)were used to interpret calcareous nannofossils The Nannotax web-site (httpinatmsocorgNannotax3) was consulted to find up-dated nannofossil genera and species ranges The identifiedbioevents for both fossil groups were calibrated to the GPTS (Grad-stein et al 2012) for consistency with the methods described inPaleomagnetism (see Age model Figure F17 Tables T12 T13)

All data were recorded in the DESClogik spreadsheet program anduploaded into the LIMS database

The core catcher (CC) sample of each core was examined Addi-tional samples were taken from the working halves as necessary torefine the biostratigraphy preferentially sampling tuffaceousmudmudstone intervals

As the core catcher is 5 cm long and neither the orientation northe precise position of a studied sample within is available the meandepth for any identified bioevent (ie T = top and B = bottom) iscalculated following the scheme in Figure F15

ForaminifersSediment volumes of 10 cm3 were taken Generally this volume

yielded sufficient numbers of foraminifers (~300 specimens persample) with the exception of those from the volcaniclastic-rich in-tervals where intense dilution occurred All samples were washedover a 63 μm mesh sieve rinsed with DI water and dried in an ovenat 50degC Samples that were more lithified were soaked in water anddisaggregated using a shaking table for several hours If necessarythe samples were soaked in warm (70degC) dilute hydrogen peroxide(20) for several hours prior to wet sieving For the most lithifiedsamples we used a kerosene bath to saturate the pores of each driedsample following the method presented by Hermann (1992) for sim-ilar material recovered during Leg 126 All dry coarse fractions wereplaced in a labeled vial ready for micropaleontological examinationCross contamination between samples was avoided by ultrasoni-cally cleaning sieves between samples Where coarse fractions werelarge relative abundance estimates were made on split samples ob-tained using a microsplitter as appropriate

Examination of foraminifers was carried out on the gt150 μmsize fraction following dry sieving The sample was spread on a sam-ple tray and examined for planktonic foraminifer datum diagnosticspecies We made a visual assessment of group and species relativeabundances as well as their preservation according to the categoriesdefined below Micropaleontological reference slides were assem-bled for some samples where appropriate for the planktonic faunasamples and for all benthic fauna samples These are marked by anasterisk next to the sample name in the results table Photomicro-graphs were taken using a Spot RTS system with IODP Image Cap-ture and commercial Spot software

The proportion of planktonic foraminifers in the gt150 μm frac-tion (ie including lithogenic particles) was estimated as follows

B = barren (no foraminifers present)R = rare (lt10)C = common (10ndash30)A = abundant (gt30)

The proportion of benthic foraminifers in the biogenic fractiongt150 μm was estimated as follows

B = barren (no foraminifers present)R = rare (lt1)F = few (1ndash5)C = common (gt5ndash10)A = abundant (gt10ndash30)D = dominant (gt30)

The relative abundance of foraminifer species in either theplanktonic or benthic foraminifer assemblages (gt150 μm) were esti-mated as follows



Table T12 Calcareous nannofossil datum events used for age estimates T = top B = bottom Tc = top common occurrence Bc = bottom common occurrence(Continued on next two pages) Download table in csv format

ZoneSubzone

base Planktonic foraminifer datumGTS2012age (Ma)

Published error (Ma) Source

T Globorotalia flexuosa 007 Gradstein et al 2012T Globigerinoides ruber (pink) 012 Wade et al 2011B Globigerinella calida 022 Gradstein et al 2012B Globigerinoides ruber (pink) 040 Li 1997B Globorotalia flexuosa 040 Gradstein et al 2012B Globorotalia hirsuta 045 Gradstein et al 2012

Pt1b T Globorotalia tosaensis 061 Gradstein et al 2012B Globorotalia hessi 075 Gradstein et al 2012T Globoturborotalita obliquus 130 plusmn001 Gradstein et al 2012T Neogloboquadrina acostaensis 158 Gradstein et al 2012T Globoturborotalita apertura 164 plusmn003 Gradstein et al 2012

Pt1a T Globigerinoides fistulosus 188 plusmn003 Gradstein et al 2012T Globigerinoides extremus 198 Gradstein et al 2012B Pulleniatina finalis 204 plusmn003 Gradstein et al 2012T Globorotalia pertenuis 230 Gradstein et al 2012T Globoturborotalita woodi 230 plusmn002 Gradstein et al 2012

PL6 T Globorotalia pseudomiocenica 239 Gradstein et al 2012B Globorotalia truncatulinoides 258 Gradstein et al 2012T Globoturborotalita decoraperta 275 plusmn003 Gradstein et al 2012T Globorotalia multicamerata 298 plusmn003 Gradstein et al 2012B Globigerinoides fistulosus 333 Gradstein et al 2012B Globorotalia tosaensis 335 Gradstein et al 2012

PL5 T Dentoglobigerina altispira 347 Gradstein et al 2012B Globorotalia pertenuis 352 plusmn003 Gradstein et al 2012

PL4 T Sphaeroidinellopsis seminulina 359 Gradstein et al 2012T Pulleniatina primalis 366 Wade et al 2011T Globorotalia plesiotumida 377 plusmn002 Gradstein et al 2012

PL3 T Globorotalia margaritae 385 Gradstein et al 2012T Pulleniatina spectabilis 421 Wade et al 2011B Globorotalia crassaformis sensu lato 431 plusmn004 Gradstein et al 2012

PL2 T Globoturborotalita nepenthes 437 plusmn001 Gradstein et al 2012T Sphaeroidinellopsis kochi 453 Gradstein et al 2012T Globorotalia cibaoensis 460 Gradstein et al 2012T Globigerinoides seigliei 472 Gradstein et al 2012B Spheroidinella dehiscens sensu lato 553 plusmn004 Gradstein et al 2013

PL1 B Globorotalia tumida 557 Gradstein et al 2012B Turborotalita humilis 581 plusmn017 Gradstein et al 2012T Globoquadrina dehiscens 592 Gradstein et al 2012B Globorotalia margaritae 608 plusmn003 Gradstein et al 2012

M14 T Globorotalia lenguaensis 614 Gradstein et al 2012B Globigerinoides conglobatus 620 plusmn041 Gradstein et al 2012T Globorotalia miotumida (conomiozea) 652 Gradstein et al 2012B Pulleniatina primalis 660 Gradstein et al 2012B Globorotalia miotumida (conomiozea) 789 Gradstein et al 2012B Candeina nitida 843 plusmn004 Gradstein et al 2012B Neogloboquadrina humerosa 856 Gradstein et al 2012

M13b B Globorotalia plesiotumida 858 plusmn003 Gradstein et al 2012B Globigerinoides extremus 893 plusmn003 Gradstein et al 2012B Globorotalia cibaoensis 944 plusmn005 Gradstein et al 2012B Globorotalia juanai 969 Gradstein et al 2012

M13a B Neogloboquadrina acostaensis 979 Chaisson and Pearson 1997T Globorotalia challengeri 999 Gradstein et al 2012

M12 T Paragloborotalia mayerisiakensis 1046 plusmn002 Gradstein et al 2012B Globorotalia limbata 1064 plusmn026 Gradstein et al 2012T Cassigerinella chipolensis 1089 Gradstein et al 2012B Globoturborotalita apertura 1118 plusmn013 Gradstein et al 2012B Globorotalia challengeri 1122 Gradstein et al 2012B regular Globigerinoides obliquus 1125 Gradstein et al 2012B Globoturborotalita decoraperta 1149 Gradstein et al 2012T Globigerinoides subquadratus 1154 Gradstein et al 2012

M11 B Globoturborotalita nepenthes 1163 plusmn002 Gradstein et al 2012M10 T Fohsella fohsi Fohsella plexus 1179 plusmn015 Lourens et al 2004

T Clavatorella bermudezi 1200 Gradstein et al 2012B Globorotalia lenguanensis 1284 plusmn005 Gradstein et al 2012B Sphaeroidinellopsis subdehiscens 1302 Gradstein et al 2012

M9b B Fohsella robusta 1313 plusmn002 Gradstein et al 2012T Cassigerinella martinezpicoi 1327 Gradstein et al 2012



M9a B Fohsella fohsi 1341 plusmn004 Gradstein et al 2012B Neogloboquadrina nympha 1349 Gradstein et al 2012

M8 B Fohsella praefohsi 1377 Gradstein et al 2012T Fohsella peripheroronda 1380 Gradstein et al 2012T Globorotalia archeomenardii 1387 Gradstein et al 2012

M7 B Fohsella peripheroacuta 1424 Gradstein et al 2012B Globorotalia praemenardii 1438 Gradstein et al 2012T Praeorbulina sicana 1453 Gradstein et al 2012T Globigeriantella insueta 1466 Gradstein et al 2012T Praeorbulina glomerosa sensu stricto 1478 Gradstein et al 2012T Praeorbulina circularis 1489 Gradstein et al 2012

M6 B Orbulina suturalis 1510 Gradstein et al 2012B Clavatorella bermudezi 1573 Gradstein et al 2012B Praeorbulina circularis 1596 Gradstein et al 2012B Globigerinoides diminutus 1606 Gradstein et al 2012B Globorotalia archeomenardii 1626 Gradstein et al 2012

M5b B Praeorbulina glomerosa sensu stricto 1627 Gradstein et al 2012B Praeorbulina curva 1628 Gradstein et al 2012

M5a B Praeorbulina sicana 1638 Gradstein et al 2012T Globorotalia incognita 1639 Gradstein et al 2012

M4b B Fohsella birnageae 1669 Gradstein et al 2012B Globorotalia miozea 1670 Gradstein et al 2012B Globorotalia zealandica 1726 Gradstein et al 2012T Globorotalia semivera 1726 Gradstein et al 2012

M4a T Catapsydrax dissimilis 1754 Gradstein et al 2012B Globigeriantella insueta sensu stricto 1759 Gradstein et al 2012B Globorotalia praescitula 1826 Gradstein et al 2012T Globiquadrina binaiensis 1909 Gradstein et al 2012

M3 B Globigerinatella sp 1930 Gradstein et al 2012B Globiquadrina binaiensis 1930 Gradstein et al 2012B Globigerinoides altiaperturus 2003 Gradstein et al 2012T Tenuitella munda 2078 Gradstein et al 2012B Globorotalia incognita 2093 Gradstein et al 2012T Globoturborotalita angulisuturalis 2094 Gradstein et al 2012

M2 T Paragloborotalia kugleri 2112 Gradstein et al 2012T Paragloborotalia pseudokugleri 2131 Gradstein et al 2012B Globoquadrina dehiscens forma spinosa 2144 Gradstein et al 2012T Dentoglobigerina globularis 2198 Gradstein et al 2012

M1b B Globoquadrina dehiscens 2244 Gradstein et al 2012T Globigerina ciperoensis 2290 Gradstein et al 2012B Globigerinoides trilobus sensu lato 2296 Gradstein et al 2012

M1a B Paragloborotalia kugleri 2296 Gradstein et al 2012T Globigerina euapertura 2303 Gradstein et al 2012T Tenuitella gemma 2350 Gradstein et al 2012Bc Globigerinoides primordius 2350 Gradstein et al 2012

O7 B Paragloborotalia pseudokugleri 2521 Gradstein et al 2012B Globigerinoides primordius 2612 Gradstein et al 2012

O6 T Paragloborotalia opima sensu stricto 2693 Gradstein et al 2012O5 Tc Chiloguembelina cubensis 2809 Gradstein et al 2012O4 B Globigerina angulisuturalis 2918 Gradstein et al 2013

B Tenuitellinata juvenilis 2950 Gradstein et al 2012T Subbotina angiporoides 2984 Gradstein et al 2012

O3 T Turborotalia ampliapertura 3028 Gradstein et al 2012B Paragloborotalia opima 3072 Gradstein et al 2012

O2 T Pseudohastigerina naguewichiensis 3210 Gradstein et al 2012B Cassigerinella chipolensis 3389 Gradstein et al 2012Tc Pseudohastigerina micra 3389 Gradstein et al 2012

O1 T Hantkenina spp Hantkenina alabamensis 3389 Gradstein et al 2012T Turborotalia cerroazulensis 3403 Gradstein et al 2012T Cribrohantkenina inflata 3422 Gradstein et al 2012

E16 T Globigerinatheka index 3461 Gradstein et al 2012T Turborotalia pomeroli 3566 Gradstein et al 2012B Turborotalia cunialensis 3571 Gradstein et al 2012B Cribrohantkenina inflata 3587 Gradstein et al 2012

E15 T Globigerinatheka semiinvoluta 3618 Gradstein et al 2012T Acarinina spp 3775 Gradstein et al 2012T Acarinina collactea 3796 Gradstein et al 2012T Subbotina linaperta 3796 Gradstein et al 2012

ZoneSubzone



Table T12 (continued) (Continued on next page)



E14 T Morozovelloides crassatus 3825 Gradstein et al 2012T Acarinina mcgowrani 3862 Gradstein et al 2012B Globigerinatheka semiinvoluta 3862 Gradstein et al 2012T Planorotalites spp 3862 Gradstein et al 2012T Acarinina primitiva 3912 Gradstein et al 2012T Turborotalia frontosa 3942 Gradstein et al 2012

E13 T Orbulinoides beckmanni 4003 Gradstein et al 2012

ZoneSubzone




Table T13 Planktonic foraminifer datum events used for age estimates = age calibrated by Gradstein et al (2012) timescale (GTS2012) for the equatorialPacific B = bottom Bc = bottom common T = top Tc = top common Td = top dominance Ba = bottom acme Ta = top acme X = abundance crossover (Con-tinued on next page) Download table in csv format

ZoneSubzone

base Calcareous nannofossils datumGTS2012 age

(Ma)

X Gephyrocapsa caribbeanicandashEmiliania huxleyi 009CN15 B Emiliania huxleyi 029CN14b T Pseudoemiliania lacunosa 044

Tc Reticulofenestra asanoi 091Td small Gephyrocapsa spp 102B Gephyrocapsa omega 102

CN14a B medium Gephyrocapsa spp reentrance 104Bc Reticulofenestra asanoi 114T large Gephyrocapsa spp 124Bd small Gephyrocapsa spp 124T Helicosphaera sellii 126B large Gephyrocapsa spp 146T Calcidiscus macintyrei 160

CN13b B medium Gephyrocapsa spp 173CN13a T Discoaster brouweri 193

T Discoaster triradiatus 195Ba Discoaster triradiatus 222

CN12d T Discoaster pentaradiatus 239CN12c T Discoaster surculus 249CN12b T Discoaster tamalis 280

T Sphenolithus spp 365CN12a T Reticulofenestra pseudoumbilicus 370

T Amaurolithus tricornulatus 392Bc Discoaster brouweri 412

CN11b Bc Discoaster asymmetricus 413CN11a T Amourolithus primus 450

T Ceratolithus acutus 504CN10c B Ceratolithus rugosus 512

T Triquetrorhabdulus rugosus 528B Ceratolithus larrymayeri 534

CN10b B Ceratolithus acutus 535T Discoaster quinqueramus 559

CN9d T Nicklithus amplificus 594X Nicklithus amplificusndashTriquetrorhabdulus rugosus 679

CN9c B Nicklithus amplificus 691CN9b B Amourolithus primus Amourolithus spp 742

Bc Discoaster loeblichii 753Bc Discoaster surculus 779B Discoaster quinqueramus 812

CN9a B Discoaster berggrenii 829T Minylitha convallis 868B Discoaster loeblichii 877Bc Reticulofenestra pseudoumbilicus 879T Discoaster bollii 921Bc Discoaster pentaradiatus 937

CN8 T Discoaster hamatus 953T Catinaster calyculus 967

T Catinaster coalitus 969B Minylitha convallis 975X Discoaster hamatusndashDiscoaster noehamatus 976B Discoaster bellus 1040X Catinaster calyculusndashCatinaster coalitus 1041B Discoaster neohamatus 1052

CN7 B Discoaster hamatus 1055Bc Helicosphaera stalis 1071Tc Helicosphaera walbersdorfensis 1074B Discoaster brouweri 1076B Catinaster calyculus 1079

CN6 B Catinaster coalitus 1089T Coccolithus miopelagicus 1097T Calcidiscus premacintyrei 1121Tc Discoaster kugleri 1158T Cyclicargolithus floridanus 1185

CN5b Bc Discoaster kugleri 1190T Coronocyclus nitescens 1212Tc Calcidiscus premacintyrei 1238Bc Calcidiscus macintyrei 1246B Reticulofenestra pseudoumbilicus 1283B Triquetrorhabdulus rugosus 1327Tc Cyclicargolithus floridanus 1328B Calcidiscus macintyrei 1336

CN5a T Sphenolithus heteromorphus 1353T Helicosphaera ampliaperta 1491Ta Discoaster deflandrei group 1580B Discoaster signus 1585B Sphenolithus heteromorphus 1771

CN3 T Sphenolithus belemnos 1795CN2 T Triquetrorhabdulus carinatus 1828

B Sphenolithus belemnos 1903B Helicosphaera ampliaperta 2043X Helicosphaera euprhatisndashHelicosphaera carteri 2092Bc Helicosphaera carteri 2203T Orthorhabdulus serratus 2242B Sphenolithus disbelemnos 2276

CN1c B Discoaster druggi (sensu stricto) 2282T Sphenolithus capricornutus 2297T Sphenolithus delphix 2311

CN1a-b T Dictyococcites bisectus 2313B Sphenolithus delphix 2321T Zygrhablithus bijugatus 2376T Sphenolithus ciperoensis 2443Tc Cyclicargolithus abisectus 2467X Triquetrorhabdulus lungusndashTriquetrorhabdulus carinatus 2467T Chiasmolithus altus 2544

ZoneSubzone


(Ma)



T = trace (lt01 of species in the total planktonicbenthic fora-minifer assemblage gt150 μm)

P = present (lt1)R = rare (1ndash5)F = few (gt5ndash10)A = abundant (gt10ndash30)D = dominant (gt30)

The degree of fragmentation of the planktonic foraminifers(gt150 μm) where a fragment was defined as part of a planktonic for-aminifer shell representing less than half of a whole test was esti-mated as follows

N = none (no planktonic foraminifer fragment observed in the gt150 μm fraction)

L = light (0ndash10)M = moderate (gt10ndash30)S = severe (gt30ndash50)VS = very severe (gt 50)

A record of the preservation of the samples was made usingcomments on the aspect of the whole planktonic foraminifer shells(gt150 μm) examined

E = etched (gt30 of planktonic foraminifer assemblage shows etching)

G = glassy (gt50 of planktonic foraminifers are translucent)F = frosty (gt50 of planktonic foraminifers are not translucent)

As much as possible we tried to give a qualitative estimate of theextent of reworking andor downhole contamination using the fol-lowing scale

L = lightM = moderateS = severe

Calcareous nannofossilsCalcareous nannofossil assemblages were examined and de-

scribed from smear slides made from core catcher samples of eachrecovered core Standard smear slide techniques were utilized forimmediate biostratigraphic examination For coarse material thefine fraction was separated from the coarse fraction by settlingthrough water before the smear slide was prepared All sampleswere examined using a Zeiss Axiophot light microscope with an oilimmersion lens under a magnification of 1000times The semiquantita-tive abundances of all species encountered were described (see be-low) Additional observations with the scanning electronmicroscope (SEM) were used to identify Emiliania huxleyi Photo-micrographs were taken using a Spot RTS system with Image Cap-ture and Spot software

The Nannotax website (httpinatmsocorgNannotax3) wasconsulted to find up-to-date nannofossil genera and species rangesThe genus Gephyrocapsa has been divided into species however inaddition as the genus shows high variations in size it has also beendivided into three major morphogroups based on maximum cocco-lith length following the biometric subdivision by Raffi et al (1993)and Raffi et al (2006) small Gephyrocapsa (lt4 μm) medium Geph-yrocapsa (4ndash55 μm) and large Gephyrocapsa spp (gt55 μm)

Species abundances were determined using the criteria definedbelow

V = very abundant (gt100 specimens per field of view)A = abundant (gt10ndash100 specimens per field of view)C = common (gt1ndash10 specimens per field of view)F = few (gt1ndash10 specimens per 2ndash10 fields of view)VF = very few (1 specimen per 2ndash10 fields of view)R = rare (1 specimen per gt10 fields of view)B = barren (no nannofossils) (reworked) = reworked occurrence

The following basic criteria were used to qualitatively provide ameasure of preservation of the nannofossil assemblage

E = excellent (no dissolution is seen all specimens can be identi-fied)

G = good (little dissolution andor overgrowth is observed diag-nostic characteristics are preserved and all specimens can be identified)

M = moderate (dissolution andor overgrowth are evident a sig-nificant proportion [up to 25] of the specimens cannot be identified to species level with absolute certainty)

Bc Triquetrorhabdulus carinatus 2657CP19b T Sphenolithus distentus 2684

T Sphenolithus predistentus 2693T Sphenolithus pseudoradians 2873

CP19a B Sphenolithus ciperoensis 2962CP18 B Sphenolithus distentus 3000CP17 T Reticulofenestra umbilicus 3202CP16c T Coccolithus formosus 3292CP16b Ta Clausicoccus subdistichus 3343CP16a T Discoaster saipanensis 3444

T Discoaster barbadiensis 3476T Dictyococcites reticulatus 3540B Isthmolithus recurvus 3697B Chiasmolithus oamaruensis 3732

CP15 T Chiasmolithus grandis 3798B Chiasmolithus oamaruensis 3809B Dictyococcites bisectus 3825

CP14b T Chiasmolithus solitus 4040

ZoneSubzone


(Ma)


Figure F15 Scheme adopted to calculate the mean depth for foraminiferand nannofossil bioevents

T

CC n

CC n+1

Case I B = bottom synonymousof first appearance of aspecies (+) observed in CC n

Case II T = top synonymous oflast appearance of aspecies (-) observed in CC n+1

B

CC n

CC n+1

1680

1685

2578

2583

+6490

6495

6500

6505



P = poor (severe dissolution fragmentation andor overgrowth has occurred most primary features have been destroyed and many specimens cannot be identified at the species level)

For each sample a comment on the presence or absence of dia-toms and siliceous plankton is recorded

Age modelOne of the main goals of Expedition 350 was to establish an ac-

curate age model for Sites U1436 and U1437 in order to understandthe temporal evolution of the Izu arc Both biostratigraphers andpaleomagnetists worked closely to deliver a suitable shipboard agemodel

TimescaleThe polarity stratigraphy established onboard was correlated

with the GPTS of Gradstein et al (2012) The biozones for plank-tonic foraminifers and calcareous nannofossils and the paleomag-netic chrons were calibrated according to this GPTS (Figure F16Tables T11 T12 T13) Because of calibration uncertainties in theGPTS the age model is based on a selection of tie points rather thanusing all biostratigraphic datums This approach minimizes spuri-ous variations in estimating sedimentation rates Ages and depthrange for the biostratigraphic and magnetostratigraphic datums areshown in Tables T11 T12 and T13

Depth scaleSeveral depth scale types are defined by IODP based on tools

and computation procedures used to estimate and correlate the

depth of core samples (see Operations) Because only one hole wascored at Site U1436 the three holes cored at Site U1437 did notoverlap by more than a few meters and instances of gt100 recoverywere very few at both sites we used the standard CSF-A depth scalereferred to as mbsf in this volume

Constructing the age-depth modelIf well-constrained by biostratigraphic data the paleomagnetic

data were given first priority to construct the age model The nextpriority was given to calcareous nannofossils followed by plank-tonic foraminifers In cases of conflicting microfossil datums wetook into account the reliability of individual datums as global dat-ing tools in the context of the IBM rear arc as follows

1 The reliability of fossil groups as stratigraphic indicators varies according to the sampling interval and nature of the material collected (ie certain intervals had poor microfossil recovery)

2 Different datums can contradict each other because of contrast-ing abundances preservation localized reworking during sedi-mentation or even downhole contamination during drilling The quality of each datum was assessed by the biostratigraphers

3 The uncertainties associated with bottom or top datums were considered Bottom datums are generally preferred as they are considered to be more reliable to secure good calibrations to GPTS 2012

The precision of the shipboard Expedition 350 site-specific age-depth models is limited by the generally low biostratigraphic sam-pling resolution (45ndash9 m) The procedure applied here resulted inconservative shipboard age models satisfying as many constraintsas possible without introducing artifacts Construction of the age-depth curve for each site started with a plot of all biostratigraphic

Figure F16 Expedition 350 timescale based on calcareous nannofossil and planktonic foraminifer zones and datums B = bottom T = top Bc = bottom com-mon Tc = top common Bd = bottom dominance Td = top dominance Ba = bottom acme Ta = top acme X = crossover in nannofossils A Quaternary toPliocene (0ndash53 Ma) (Continued on next three pages)

Age

(M

a)

Planktonicforaminifers DatumEvent (Ma) Secondary datumEvent (Ma)

Calcareousnannofossils

05

0

1

15

2

25

3

35

4

45

5

Qua

tern

ary

Plio

cene

Ple

isto

cene

Hol

Zan

clea

nP

iace

nzia

nG

elas

ian

Cal

abria

nIo

nian

Taran-tian

C3n

C2An

C2Ar

C2n

C2r

C1n

C1r

B Globorotalia truncatulinoides (193)

T Globorotalia tosaensis (061)

T Globigerinoides fistulosus (188)

T Globorotalia pseudomiocenica [Indo-Pacific] (239)

T Dentoglobigerina altispira [Pacific] (347)T Sphaeroidinellopsis seminulina [Pacific] (359)

T Globoturborotalita nepenthes (437)

B Globigerinella calida (022)B Globorotalia flexuosa (040)

B Globorotalia hirsuta (045)B Globorotalia hessi (075)

B Globigerinoides fistulosus (333)

B Globorotalia crassaformis sl (431)

T Globorotalia flexuosa (007)

B Globigerinoides extremus (198)

T Globorotalia pertenuis (230)

T Globoturborotalita decoraperta (275)

T Globorotalia multicamerata (298)

T Pulleniatina primalis (366)

T Pulleniatina spectabilis [Pacific] (421)

T Globorotalia cibaoensis (460)

PL1

PL2

PL3PL4

PL5

PL6

Pt1

a

b

N18 N19

N20 N21

N22

B Emiliania huxleyi (029)

B Gephyrocapsa spp gt4 microm reentrance (104)

B Gephyrocapsa spp gt4 microm (173)

Bc Discoaster asymmetricus (413)

B Ceratolithus rugosus (512)

T Pseudoemiliania lacunosa (044)

T Discoaster brouweri (193)

T Discoaster pentaradiatus (239)

T Discoaster surculus (249)

T Discoaster tamalis (280)

T Reticulofenestra pseudoumbilicus (370)

T Amaurolilthus tricorniculatus (392)

T Amaurolithus primus (450)

Ba Discoaster triradiatus (222)

Bc Discoaster brouweri (412)

Tc Reticulofenestra asanoi (091)

Bc Reticulofenestra asanoi (114)

T Helicosphaera sellii (126)T Calcidiscus macintyrei (160)

T Discoaster triradiatus (195)

T Sphenolithus spp (354)

T Reticulofenestra antarctica (491)T Ceratolithus acutus (504)

T Triquetrorhabdulus rugosus (528)

X Geph caribbeanica -gt Emiliania huxleyi (009)

B Gephyrocapsa omega (102)Td Gephyrocapsa spp small (102)

Bd Gephyrocapsa spp small (124)T Gephyrocapsa spp gt55 microm (124)


NN12

NN13

NN14NN15

NN16

NN17

NN18

NN19

NN20

NN21

CN10

CN11

CN12

CN13

CN14

CN15

b

c

a

b

a

b

c

d

a

b

a

b

1

2

1

2

1

2

3

1

2

34

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)

Okada andBukry(1980)

Neo

gene

T Globigerinoides ruber pink (012)

B Globigerinoides ruber pink (04)

TGloboturborotalita obliquus (13)T Neogloboquadrina acostaensis (158)T Globoturborotalita aperta (164)

B Pulleniatina finalis (204)

TGloboturborotalita woodi (23)

T Globorotalia truncatulinoides (258)

B Globorotalia tosaensis (335)B Globorotalia pertenuis (352)

TGloborotalia plesiotumida (377)TGloborotalia margaritae (385)

T Spheroidinellopsis kochi (453)

A Quaternary - Neogene

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr

on



Figure F16 (continued) B Late to Middle Miocene (53ndash14 Ma) (Continued on next page)

Age

(M

a)

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr

on Planktonicforaminifers DatumEvent (Ma) Secondary DatumEvent (Ma)


55

6

65

7

75

8

85

9

95

10

105

11

115

12

125

13

135

14

Neo

gene

Mio

cene

Ser

rava

llian

Tort

onia

nM

essi

nian

C5ACn

C5ABnC5ABr

C5AAnC5AAr

C5An

C5Ar

C5n

C5r

C4An

C4Ar

C4r

C4n

C3BnC3Br

C3An

C3Ar

C3rB Globorotalia tumida [Pacific] (557)

B Globorotalia plesiotumida (858)

B Neogloboquadrina acostaensis [subtropical] (983)

B Neogloboquadrina acostaensis [temperate] (1057)

B Globoturborotalita nepenthes (1163)

B Fohsella robusta (1313)

B Fohsella fohsi (1341)

B Fohsella praefohsi (1377)

T Globoquadrina dehiscens (592)

T Globorotalia lenguaensis [Pacific] (614)

T Paragloborotalia mayeri [subtropical] (1046)

T Paragloborotalia mayerisiakensis [subtropical] (1046)

T Fohsella fohsi Fohsella plexus (1179)

B Sphaeroidinellopsis dehiscens sl (553)

B Globorotalia margaritae (608)

B Pulleniatina primalis (660)

B Neogloboquadrina humerosa (856)


B Globorotalia cibaoensis (944)

B Globorotalia juanai (969)

B Globoturborotalita apertura (1118)

B Globoturborotalita decoraperta (1149)

B Globorotalia lenguanensis (1284)B Sphaeroidinellopsis subdehiscens (1302)B Fohsella robusta (1313)

Tr Globigerinoides obliquus (1125)

T Globigerinoides subquadratus (1154)

T Cassigerinella martinezpicoi (1327)

T Fohsella peripheroronda (1380)Tr Clavatorella bermudezi (1382)T Globorotalia archeomenardii (1387)M7

M8

M9

M10

M11

M12

M13

M14

a

b

a

b

a

b

N10

N11

N12

N13

N14

N15

N16

N17

B Ceratolithus acutus (535)

B Nicklithus amplificus (691)

B Amaurolithus primus Amaurolithus spp (742)

B Discoaster quinqueramus (812)

T Discoaster quinqueramus (559)

B Discoaster berggrenii (829)

B Discoaster hamatus (1055)

B Catinaster coalitus (1089)

Bc Discoaster kugleri (1190)

T Nicklithus amplificus (594)

T Discoaster hamatus (953)

T Sphenolithus heteromorphus (1353)

X Nicklithus amplificus -gt Triquetrorhabdulus rugosus (679)

Bc Discoaster surculus (779)

B Discoaster loeblichii (877)Bc Reticulofenestera pseudoumbilicus (879)

Bc Discoaster pentaradiatus (937)

B Minylitha convallis (975) X Discoaster hamatus -gt D neohamatus (976)

B Discoaster bellus (1040)X Catinaster calyculus -gt C coalitus (1041) B Discoaster neohamatus (1055)

Bc Helicosphaera stalis (1071)

B Discoaster brouweri (1076)B Catinaster calyculus (1079)

Bc Calcidiscus macintyrei (1246)

B Reticulofenestra pseudoumbilicus (1283)

B Triquetrorhabdulus rugosus (1327)

B Calcidiscus macintyrei (1336)

T Discoaster loeblichii (753)

T Minylitha convallis (868)

T Discoaster bollii (921)

T Catinaster calyculus (967)T Catinaster coalitus (969)

Tc Helicosphaera walbersdorfensis (1074)

T Coccolithus miopelagicus (1097)

T Calcidiscus premacintyrei (1121)

Tc Discoaster kugleri (1158)T Cyclicargolithus floridanus (1185)

T Coronocyclus nitescens (1212)

Tc Calcidiscus premacintyrei (1238)

Tc Cyclicargolithus floridanus (1328)

B Ceratolithus larrymayeri (sp 1) (534)

NN5

NN6

NN7

NN8

NN9

NN10

NN11

NN12

CN4

CN5

CN6

CN7

CN8

CN9

a

b

a

b

c

d

a

1

1

2

1

2

1

2

1

2

1

2

1

2

1

2

3

3

1

2

2

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)


B Turborotalita humilis (581)

B Globigerinoides conglobatus (62)

T Globorotalia miotumida (conomiozea) (652)

B Globorotalia miotumida (conomiozea) (789)

B Candeina nitida (843)

T Globorotalia challengeri (999)

B Globorotalia limbata (1064)

T Cassigerinella chipolensis (1089)

B Globorotalia challengeri (1122)

T Clavatorella bermudezi (12)

B Neogene

and paleomagnetic control points Age and depth uncertaintieswere represented by error bars Obvious outliers and conflicting da-tums were then masked until the line connecting the remainingcontrol points was contiguous (ie without age-depth inversions) inorder to have linear correlation Next an interpolation curve wasapplied that passed through all control points Linear interpolationis used for the simple age-depth relationships

Linear sedimentation ratesBased on the age-depth model linear sedimentation rates

(LSRs) were calculated and plotted based on a subjective selectionof time slices along the age-depth model Keeping in mind the arbi-trary nature of the interval selection only the most realistic andconservative segments were used Hiatuses were inferred when theshipboard magnetostratigraphy and biostratigraphy could not becontinuously correlated LSRs are expressed in meters per millionyears

Mass accumulation ratesMass accumulation rate (MAR) is obtained by simple calcula-

tion based on LSR and dry bulk density (DBD) averaged over theLSR defined DBD is derived from shipboard MAD measurements(see Physical properties) Average values for DBD carbonate accu-mulation rate (CAR) and noncarbonate accumulation rate (nCAR)were calculated for the intervals selected for the LSRs CAR andnCAR are expressed in gcm2ky and calculated as follows

MAR (gcm2ky) = LSR (cmky) times DBD (gcm3)

CAR = CaCO3 (fraction) times MAR

and

nCAR = MAR minus CAR

A step plot of LSR total MAR CAR and nCAR is presented ineach site chapter


jim
Highlight
jim
Highlight
jim
Highlight
jim
Highlight


Figure F16 (continued) C Middle to Early Miocene (14ndash23 Ma) (Continued on next page)

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr

on Planktonicforaminifers DatumEvent (Ma) Secondary datumEvent (Ma)


14

145

15

155

16

165

17

175

18

185

19

195

20

205

21

215

22

225

23

Neo

gene

Mio

cene

Aqu

itani

anB

urdi

galia

nLa

nghi

an

C6Cn

C6Bn

C6Br

C6AAn

C6AAr

C6Ar

C6An

C6n

C6r

C5En

C5Er

C5Dr

C5Dn

C5Cr

C5Cn

C5Br

C5Bn

C5ADn

C5ADr

C5ACrB Fohsella peripheroacuta (1424)

B Orbulina suturalis (1510)

B Praeorbulina glomerosa ss (1627)B Praeorbulina sicana (1638)

B Globigerinatella insueta ss (1759)

B Globigerinatella sp (1930)

B Globoquadrina dehiscens forma spinosa (2244)

B Globoquadrina dehiscens forma spinosa (2144)B Globoquadrina dehiscens (2144)

T Dentoglobigerina globularis (2198)

B Globigerinoides trilobus sl (2296)B Paragloborotalia kugleri (2296)

T Catapsydrax dissimilis (1754)

T Paragloborotalia kugleri (2112)

B Globorotalia praemenardii (1438)

B Clavatorella bermudezi (1573)

B Praeorbulina circularis (1596)

B Globorotalia archeomenardii (1626)B Praeorbulina curva (1628)

B Fohsella birnageae (1669)

B Globorotalia zealandica (1726)

B Globorotalia praescitula (1826)

B Globoquadrina binaiensis (1930)

T Globoquadrina binaiensis (1909)

B Globigerinoides altiaperturus (2003)

T Praeorbulina sicana (1453)T Globigerinatella insueta (1466)T Praeorbulina glomerosa ss (1478)T Praeorbulina circularis (1489)

T Tenuitella munda (2078)

T Globoturborotalita angulisuturalis (2094)T Paragloborotalia pseudokugleri (2131)

T Globigerina ciperoensis (2290)

M1

M2

M3

M4

M5

M6

M7

a

b

a

b

a

b

N4

N5

N6

N7

N8

N9

N10

B Sphenolithus belemnos (1903)

T Sphenolithus belemnos (1795)

B Discoaster druggi ss (2282)

T Helicosphaera ampliaperta (1491)

T Triquetrorhabdulus carinatus (1828)

B Discoaster signus (1585)

B Sphenolithus heteromorphus (1771)

B Helicosphaera ampliaperta (2043)

X Helicosphaera euphratis -gt H carteri (2092)

Bc Helicosphaera carteri (2203)

B Sphenolithus disbelemnos (2276)

Ta Discoaster deflandrei group (1580)

T Orthorhabdus serratus (2242)

T Sphenolithus capricornutus (2297)NN1

NN2

NN3

NN4

NN5

CN1

CN2

CN3

CN4

ab

c

12

1

2

1

2

1

2

1

2

1

2

12

3

3

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)


B Globigerinoides diminutus (1606)

T Globorotalia incognita (1639)

B Globorotalia miozea (167)

T Globorotalia semivera (1726)

B Globorotalia incognita (2093)

C Neogene

Age

(M

a)



Downhole measurementsWireline logging

Wireline logs are measurements of physical chemical andstructural properties of the formation surrounding a borehole thatare made by lowering probes with an electrical wireline in the holeafter completion of drilling The data are continuous with depth (atvertical sampling intervals ranging from 25 mm to 15 cm) and aremeasured in situ The sampling and depth of investigation are inter-

mediate between laboratory measurements on core samples andgeophysical surveys and provide a link for the integrated under-standing of physical properties on all scales

Logs can be interpreted in terms of stratigraphy lithology min-eralogy and geochemical composition They provide also informa-tion on the status and size of the borehole and on possibledeformations induced by drilling or formation stress When core re-covery is incomplete which is common in the volcaniclastic sedi-ments drilled during Expedition 350 log data may provide the only

Figure F16 (continued) D Paleogene (23ndash40 Ma)

23

235

24

245

25

255

26

265

27

275

28

285

29

295

30

305

31

315

32

325

33

335

34

345

35

355

36

365

37

375

38

385

39

40

395

Pal

eoge

ne

Eoc

ene

Olig

ocen

e

Bar

toni

anP

riabo

nian

Rup

elia

nC

hatti

an

C18n

C17r

C17n

C16n

C16r

C15n

C15r

C13n

C13r

C12n

C12r

C11n

C11r

C10n

C10r

C9n

C9r

C8n

C8r

C7AnC7Ar

C7n

C7r

C6Cn

C6Cr

B Paragloborotalia kugleri (2296)

B Paragloborotalia pseudokugleri (2521)

B Globigerina angulisuturalis (2918)

T Paragloborotalia opima ss (2693)

Tc Chiloguembelina cubensis (2809)

T Turborotalia ampliapertura (3028)

T Pseudohastigerina naguewichiensis (3210)

T Hantkenina alabamensis Hantkenina spp (3389)

T Globigerinatheka index (3461)

T Globigerinatheka semiinvoluta (3618)

T Morozovelloides crassatus (3825)

Bc Globigerinoides primordius (2350)T Tenuitella gemma (2350)

B Globigerinoides primordius (2612)

B Paragloborotalia opima (3072)

B Turborotalia cunialensis (3571)

B Cribrohantkenina inflata (3587)

T Cribrohantkenina inflata (3422)

B Globigerinatheka semiinvoluta (3862)


T Subbotina angiporoides (2984)

Tc Pseudohastigerina micra (3389)T Turborotalia cerroazulensis (3403)

T Turborotalia pomeroli (3566)

T Acarinina spp (3775)

T Acarinina mcgowrani (3862)

T Turborotalia frontosa (3942)

E13

E14

E15

E16

O1

O2

O3

O4

O5

O6

O7

a

P14

P15

P16 P17

P18

P19

P20

P21

P22


B Sphenolithus ciperoensis (2962)

T Sphenolithus ciperoensis (2443)

B Sphenolithus distentus (3000)

B Isthmolithus recurvus (3697)

Bc Chiasmolithus oamaruensis (3732)

B Chiasmolithus oamaruensis (rare) (3809)

T Dictyococcites bisectus gt10 microm (2313)

T Sphenolithus distentus (2684)

T Reticulofenestra umbilicus [low-mid latitude] (3202)

T Coccolithus formosus (3292)

Ta Clausicoccus subdistichus (3343)

T Discoaster saipanensis (3444)

T Discoaster barbadiensis (3476)

T Chiasmolithus grandis (3798)


B Sphenolithus delphix (2321)

X Triquetrorhabdulus longus -gtT carinatus (2467)Tc Cyclicargolithus abisectus (2467)

Bc Triquetrorhabdulus carinatus (2657)

B Dictyococcites bisectus gt10 microm (3825)

T Sphenolithus capricornutus (2297)

T Sphenolithus delphix (2311)

T Zygrhablithus bijugatus (2376)

T Chiasmolithus altus (2544)

T Sphenolithus predistentus (2693)

T Sphenolithus pseudoradians (2873)

T Reticulofenestra reticulata (3540)

NP17

NP18

NP19-NP20

NP21

NP22

NP23

NP24

NP25

NN1

CP14

CP15

CP16

CP17

CP18

CP19

b

a

b

c

ab1

2

1

2

1

2

12

1

2

1

2

1

2

1

2

3

3

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)


B Globigerinoides trilobus sl (2296)

T Globigerina euapertura (2303)

B Tenuitellinata juvenilis (2950)

B Cassigerinella chipolensis (3389)

T Subbotina linaperta (3796)

T Planorotalites spp (3862)

T Acarinina primitiva (3912)

D Paleogene

Age

(M

a)



way to characterize the formation in some intervals They can beused to determine the actual thickness of individual units or litholo-gies when contacts are not recovered to pinpoint the actual depthof features in cores with incomplete recovery or to identify intervalsthat were not recovered Where core recovery is good log and coredata complement one another and may be interpreted jointly Inparticular the imaging tools provide oriented images of the bore-hole wall that can help reorient the recovered core within the geo-graphic reference frame

OperationsLogs are recorded with a variety of tools combined into strings

Three tool strings were used during Expedition 350 (see Figure F17Tables T14 T15)

bull Triple combo with magnetic susceptibility (measuring spectral gamma ray porosity density resistivity and magnetic suscepti-bility)

bull Formation MicroScanner (FMS)-sonic (measuring spectral gamma ray sonic velocity and electrical images) and

bull Seismic (measuring gamma ray and seismic transit times)

After completion of coring the bottom of the drill string is set atsome depth inside the hole (to a maximum of about 100 mbsf) toprevent collapse of unstable shallow material In cased holes thebottom of the drill string is set high enough above the bottom of thecasing for the longest tool string to fit inside the casing The maindata are recorded in the open hole section The spectral and totalgamma ray logs (see below) provide the only meaningful data insidethe pipe to identify the depth of the seafloor

Each deployment of a tool string is a logging ldquorunrdquo starting withthe assembly of the tools and the necessary calibrations The toolstring is then sent to the bottom of the hole while recording a partialset of data and pulled back up at a constant speed typically 250ndash500mh to record the main data During each run tool strings can belowered down and pulled up the hole several times for control ofrepeatability or to try to improve the quality or coverage of the dataEach lowering or hauling up of the tool string while collecting dataconstitutes a ldquopassrdquo During each pass the incoming data are re-corded and monitored in real time on the surface system A loggingrun is complete once the tool string has been brought to the rigfloor and disassembled

Logged properties and tool measurement principlesThe main logs recorded during Expedition 350 are listed in Ta-

ble T14 More detailed information on individual tools and theirgeological applications may be found in Ellis and Singer (2007)Goldberg (1997) Lovell et al (1998) Rider (1996) Schlumberger(1989) and Serra (1984 1986 1989)

Natural radioactivityThe Hostile Environment Natural Gamma Ray Sonde (HNGS)

was used on all tool strings to measure natural radioactivity in theformation It uses two bismuth germanate scintillation detectorsand 5-window spectroscopy to determine concentrations of K Thand U whose radioactive isotopes dominate the natural radiationspectrum

The Enhanced Digital Telemetry Cartridge (EDTC see below)which is used primarily to communicate data to the surface in-cludes a sodium iodide scintillation detector to measure the totalnatural gamma ray emission It is not a spectral tool but it providesan additional high-resolution total gamma ray for each pass

PorosityFormation porosity was measured with the Accelerator Porosity

Sonde (APS) The sonde includes a minitron neutron generator thatproduces fast neutrons and 5 detectors positioned at different spac-ings from the minitron The toolrsquos detectors count neutrons that ar-rive after being scattered and slowed by collisions with atomicnuclei in the formation

The highest energy loss occurs when neutrons collide with hy-drogen nuclei which have practically the same mass as the neutronTherefore the tool provides a measure of hydrogen content whichis most commonly found in water in the pore fluid and can be di-rectly related to porosity However hydrogen may be present in sed-imentary igneous and alteration minerals which can result in anoverestimation of actual porosity

Figure F17 Wireline tool strings Expedition 350 See Table T15 for tool acro-nyms Height from the bottom is in meters VSI = Versatile Seismic Imager

Triple combo

Caliper

HLDS(density)

EDTC(telemetry

gamma ray)

HRLA(resistivity)

3986 m

3854

3656

3299

2493

1950

1600

1372

635

407367

000

Centralizer

Knuckle joints

Cablehead

Pressurebulkhead

Centralizer

MSS(magnetic

susceptibility)

FMS-sonic

DSI(acousticvelocity)

EDTC(telemetry

temperatureγ ray)

Centralizer

Cablehead

3544 m

3455

3257

2901

2673

1118

890

768

000

FMS + GPIT(resistivity image

accelerationinclinometry)

APS(porosity)

HNGS(spectral

gamma ray)

HNGS(spectral

gamma ray)

Centralizer

Seismic

VSISonde

Shuttle

1132 m

819

183

000

EDTC(telemetry

gamma ray)

Cablehead

Tool zero



Table T14 Downhole measurements made by wireline logging tool strings All tool and tool string names except the MSS are trademarks of SchlumbergerSampling interval based on optimal logging speed NA = not applicable For definitions of tool acronyms see Table T15 Download table in csv format

Tool string Tool MeasurementSampling interval

(cm)

Vertical resolution

(cm)

Depth of investigation

(cm)

Triple combo with MSS EDTC Total gamma ray 5 and 15 30 61HNGS Spectral gamma ray 15 20ndash30 61HLDS Bulk density 25 and 15 38 10APS Neutron porosity 5 and 15 36 18HRLA Resistivity 15 30 50MSS Magnetic susceptibility 254 40 20

FMS-sonic EDTC Total gamma ray 5 and 15 30 61HNGS Spectral gamma ray 15 20ndash30 61DSI Acoustic velocity 15 107 23GPIT Tool orientation and acceleration 4 15 NAFMS Microresistivity 025 1 25

Seismic EDTC Total gamma ray 5 and 15 30 61HNGS Spectral gamma ray 15 20ndash30 61VSI Seismic traveltime Stations every ~50 m NA NA

Table T15 Acronyms and units used for downhole wireline tools data and measurements Download table in csv format

Tool Output Description Unit

EDTC Enhanced Digital Telemetry CartridgeGR Total gamma ray gAPIECGR Environmentally corrected gamma ray gAPIEHGR High-resolution environmentally corrected gamma ray gAPI

HNGS Hostile Environment Gamma Ray SondeHSGR Standard (total) gamma ray gAPIHCGR Computed gamma ray (HSGR minus uranium contribution) gAPIHFK Potassium wtHTHO Thorium ppmHURA Uranium ppm

APS Accelerator Porosity SondeAPLC Neararray limestone-corrected porosity dec fractionSTOF Computed standoff inchSIGF Formation capture cross section capture units

HLDS Hostile Environment Lithodensity SondeRHOM Bulk density gcm3

PEFL Photoelectric effect barnendash

LCAL Caliper (measure of borehole diameter) inchDRH Bulk density correction gcm3

HRLA High-Resolution Laterolog Array ToolRLAx Apparent resistivity from mode x (x from 1 to 5 shallow to deep) ΩmRT True resistivity ΩmMRES Borehole fluid resistivity Ωm

MSS Magnetic susceptibility sondeLSUS Magnetic susceptibility deep reading uncalibrated units

FMS Formation MicroScannerC1 C2 Orthogonal hole diameters inchP1AZ Pad 1 azimuth degrees

Spatially oriented resistivity images of borehole wall

GPIT General Purpose Inclinometry ToolDEVI Hole deviation degreesHAZI Hole azimuth degreesFx Fy Fz Earthrsquos magnetic field (three orthogonal components) degreesAx Ay Az Acceleration (three orthogonal components) ms2

DSI Dipole Shear Sonic ImagerDTCO Compressional wave slowness μsftDTSM Shear wave slowness μsftDT1 Shear wave slowness lower dipole μsftDT2 Shear wave slowness upper dipole μsft



Upon reaching thermal energies (0025 eV) the neutrons arecaptured by the nuclei of Cl Si B and other elements resulting in agamma ray emission This neutron capture cross section (Σf ) is alsomeasured by the tool and can be used to identify such elements(Broglia and Ellis 1990 Brewer et al 1996)

DensityFormation density was measured with the Hostile Environment

Litho-Density Sonde (HLDS) The sonde contains a radioactive ce-sium (137Cs) gamma ray source and far and near gamma ray detec-tors mounted on a shielded skid which is pressed against theborehole wall by an eccentralizing arm Gamma rays emitted by thesource undergo Compton scattering where gamma rays are scat-tered by electrons in the formation The number of scatteredgamma rays that reach the detectors is proportional to the densityof electrons in the formation which is in turn related to bulk den-sity Porosity may be derived from this bulk density if the matrix(grain) density is known

The HLDS also measures photoelectric absorption as the photo-electric effect (PEF) Photoelectric absorption of the gamma raysoccurs when their energy is reduced below 150 keV after being re-peatedly scattered by electrons in the formation Because PEF de-pends on the atomic number of the elements encountered it varieswith the chemical composition of the minerals present and can beused for the identification of some minerals (Bartetzko et al 2003Expedition 304305 Scientists 2006)

Electrical resistivityThe High-Resolution Laterolog Array (HRLA) tool provides six

resistivity measurements with different depths of investigation (in-cluding the borehole fluid or mud resistivity and five measurementsof formation resistivity with increasing penetration into the forma-tion) The sonde sends a focused current beam into the formationand measures the current intensity necessary to maintain a constantdrop in voltage across a fixed interval providing direct resistivitymeasurement The array has one central source electrode and sixelectrodes above and below it which serve alternately as focusingand returning current electrodes By rapidly changing the role ofthese electrodes a simultaneous resistivity measurement isachieved at six penetration depths

Typically minerals found in sedimentary and igneous rocks areelectrical insulators whereas ionic solutions like pore water areconductors In most rocks electrical conduction occurs primarilyby ion transport through pore fluids and thus is strongly dependenton porosity Electrical resistivity can therefore be used to estimateporosity alteration and fluid salinity

Acoustic velocityThe Dipole Shear Sonic Imager (DSI) generates acoustic pulses

from various sonic transmitters and records the waveforms with anarray of 8 receivers The waveforms are then used to calculate thesonic velocity in the formation The omnidirectional monopoletransmitter emits high frequency (5ndash15 kHz) pulses to extract thecompressional velocity (VP) of the formation as well as the shear ve-locity (VS) when it is faster than the sound velocity in the boreholefluid The same transmitter can be fired in sequence at a lower fre-quency (05ndash1 kHz) to generate Stoneley waves that are sensitive tofractures and variations in permeability The DSI also has two crossdipole transmitters which allow an additional measurement ofshear wave velocity in ldquoslowrdquo formations where VS is slower than

the velocity in the borehole fluid The waveforms produced by thetwo orthogonal dipole transducers can be used to identify sonic an-isotropy that can be associated with the local stress regime

Formation MicroScannerThe FMS provides high-resolution electrical resistivity images

of the borehole walls The tool has four orthogonal arms and padseach containing 16 button electrodes that are pressed against theborehole wall during the recording The electrodes are arranged intwo diagonally offset rows of eight electrodes each A focused cur-rent is emitted from the button electrodes into the formation with areturn electrode near the top of the tool Resistivity of the formationat the button electrodes is derived from the intensity of currentpassing through the button electrodes Processing transforms thesemeasurements into oriented high-resolution images that reveal thestructures of the borehole wall Features such as flows breccia frac-tures folding or alteration can be resolved The images are orientedto magnetic north so that the dip and direction (azimuth) of planarfeatures in the formation can be estimated

Accelerometry and magnetic field measurementsAcceleration and magnetic field measurements are made with

the General Purpose Inclinometry Tool (GPIT) The primary pur-pose of this tool which incorporates a 3-component accelerometerand a 3-component magnetometer is to determine the accelerationand orientation of the FMS-sonic tool string during logging Thusthe FMS images can be corrected for irregular tool motion and thedip and direction (azimuth) of features in the FMS image can be de-termined

Magnetic susceptibilityThe magnetic susceptibility sonde (MSS) a tool designed by La-

mont-Doherty Earth Observatory (LDEO) measures the ease withwhich formations are magnetized when subjected to Earthrsquos mag-netic field This is ultimately related to the concentration and com-position (size shape and mineralogy) of magnetizable materialwithin the formation These measurements provide one of the bestmethods for investigating stratigraphic changes in mineralogy andlithology because the measurement is quick and repeatable and be-cause different lithologies often have strongly contrasting suscepti-bilities In particular volcaniclastic deposits can have a very distinctmagnetic susceptibility signature compared to hemipelagicmudmudstone The sensor used during Expedition 350 was a dual-coil sensor providing deep-reading measurements with a verticalresolution of ~40 cm The MSS was run as an addition to the triplecombo tool string using a specially developed data translation car-tridge

Auxiliary logging equipmentCablehead

The Schlumberger logging equipment head (or cablehead) mea-sures tension at the very top of the wireline tool string to diagnosedifficulties in running the tool string up or down the borehole orwhen exiting or entering the drill string or casing

Telemetry cartridgesTelemetry cartridges are used in each tool string to transmit the

data from the tools to the surface in real time The EDTC also in-cludes a sodium iodide scintillation detector to measure the totalnatural gamma ray emission of the formation which can be used tomatch the depths between the different passes and runs



Joints and adaptersBecause the tool strings combine tools of different generations

and with various designs they include several adapters and jointsbetween individual tools to allow communication provide isolationavoid interferences (mechanical or acoustic) terminate wirings orposition the tool properly in the borehole Knuckle joints in particu-lar were used to allow some of the tools such as the HRLA to remaincentralized in the borehole whereas the overlying HLDS waspressed against the borehole wall

All these additions are included and contribute to the totallength of the tool strings in Figure F17

Log data qualityThe principal factor in the quality of log data is the condition of

the borehole wall If the borehole diameter varies over short inter-vals because of washouts or ledges the logs from tools that requiregood contact with the borehole wall may be degraded Deep investi-gation measurements such as gamma ray resistivity and sonic ve-locity which do not require contact with the borehole wall aregenerally less sensitive to borehole conditions Very narrow(ldquobridgedrdquo) sections will also cause irregular log results

The accuracy of the logging depth depends on several factorsThe depth of the logging measurements is determined from thelength of the cable played out from the winch on the ship Uncer-tainties in logging depth occur because of ship heave cable stretchcable slip or even tidal changes Similarly uncertainties in the depthof the core samples occur because of incomplete core recovery orincomplete heave compensation All these factors generate somediscrepancy between core sample depths logs and individual log-ging passes To minimize the effect of ship heave a hydraulic wire-line heave compensator (WHC) was used to adjust the wirelinelength for rig motion during wireline logging operations

Wireline heave compensatorThe WHC system is designed to compensate for the vertical

motion of the ship and maintain a steady motion of the loggingtools It uses vertical acceleration measurements made by a motionreference unit located under the rig floor near the center of gravityof the ship to calculate the vertical motion of the ship It then ad-justs the length of the wireline by varying the distance between twosets of pulleys through which the wireline passes

Logging data flow and processingData from each logging run were monitored in real time and re-

corded using the Schlumberger MAXIS 500 system They were thencopied to the shipboard workstations for processing The main passof the triple combo was commonly used as a reference to whichother passes were interactively depth matched After depth match-ing all the logging depths were shifted to the seafloor after identify-ing the seafloor from a step in the gamma ray profile The electricalimages were processed by using data from the GPIT to correct forirregular tool motion and the image gains were equalized to en-hance the representation of the borehole wall All the processeddata were made available to the science party within a day of theiracquisition in ASCII format for most logs and in GIF format for theimages

The data were also transferred onshore to LDEO for a standard-ized implementation of the same data processing formatting for theonline logging database and for archiving

In situ temperature measurementsIn situ temperature measurements were made at each site using

the advanced piston corer temperature tool (APCT-3) The APCT-3fits directly into the coring shoe of the APC and consists of a batterypack data logger and platinum resistance-temperature device cali-brated over a temperature range from 0deg to 30degC Before enteringthe borehole the tool is first stopped at the seafloor for 5 min tothermally equilibrate with bottom water However the lowest tem-perature recorded during the run down was preferred to the averagetemperature at the seafloor as an estimate of the bottom water tem-perature because it is more repeatable and the bottom water is ex-pected to have the lowest temperature in the profile After the APCpenetrated the sediment it was held in place for 5ndash10 min as theAPCT-3 recorded the temperature of the cutting shoe every secondShooting the APC into the formation generates an instantaneoustemperature rise from frictional heating This heat gradually dissi-pates into the surrounding sediments as the temperature at theAPCT-3 equilibrates toward the temperature of the sediments

The equilibrium temperature of the sediments was estimated byapplying a mathematical heat-conduction model to the temperaturedecay record (Horai and Von Herzen 1985) The synthetic thermaldecay curve for the APCT-3 tool is a function of the geometry andthermal properties of the probe and the sediments (Bullard 1954Horai and Von Herzen 1985) The equilibrium temperature is esti-mated by applying an appropriate curve fitting procedure (Pribnowet al 2000) However when the APCT-3 does not achieve a fullstroke or when ship heave pulls up the APC from full penetrationthe temperature equilibration curve is disturbed and temperaturedetermination is more difficult The nominal accuracy of theAPCT-3 temperature measurement is plusmn01degC

The APCT-3 temperature data were combined with measure-ments of thermal conductivity (see Physical properties) obtainedfrom core samples to obtain heat flow values using to the methoddesigned by Bullard (1954)

ReferencesASTM International 1990 Standard method for laboratory determination of

water (moisture) content of soil and rock (Standard D2216ndash90) In Annual Book of ASTM Standards for Soil and Rock (Vol 0408) Philadel-phia (American Society for Testing Materials) [revision of D2216-63 D2216-80]

Bartetzko A Paulick H Iturrino G and Arnold J 2003 Facies reconstruc-tion of a hydrothermally altered dacite extrusive sequence evidence from geophysical downhole logging data (ODP Leg 193) Geochemistry Geo-physics Geosystems 4(10)1087 httpdxdoiorg1010292003GC000575

Berggren WA Kent DV Swisher CC III and Aubry M-P 1995 A revised Cenozoic geochronology and chronostratigraphy In Berggren WA Kent DV Aubry M-P and Hardenbol J (Eds) Geochronology Time Scales and Global Stratigraphic Correlation Special Publication - SEPM (Society for Sedimentary Geology) 54129ndash212 httpdxdoiorg102110pec95040129

Bloemendal J King JW Hall FR and Doh S-J 1992 Rock magnetism of late Neogene and Pleistocene deep-sea sediments relationship to sedi-ment source diagenetic processes and sediment lithology Journal of Geophysical Research Solid Earth 97(B4)4361ndash4375 httpdxdoiorg10102991JB03068

Blum P 1997 Physical properties handbook a guide to the shipboard mea-surement of physical properties of deep-sea cores Ocean Drilling Pro-gram Technical Note 26 httpdxdoiorg102973odptn261997



Brewer TS Harvey PK Locke J and Lovell MA 1996 Neutron absorp-tion cross section (Σ) of basaltic basement samples from Hole 896A Costa Rica rift In Alt JC Kinoshita H Stokking LB and Michael PJ (Eds) Proceedings of the Ocean Drilling Program Scientific Results 148 College Station TX (Ocean Drilling Program) 389ndash394 httpdxdoiorg102973odpprocsr1481541996

Broglia C and Ellis D 1990 Effect of alteration formation absorption and standoff on the response of the thermal neutron porosity log in gabbros and basalts examples from Deep Sea Drilling Project-Ocean Drilling Pro-gram sites Journal of Geophysical Research Solid Earth 95(B6)9171ndash9188 httpdxdoiorg101029JB095iB06p09171

Bullard EC 1954 The flow of heat through the floor of the Atlantic Ocean Proceedings of the Royal Society of London Series A Mathematical Physi-cal and Engineering Sciences 222(1150)408ndash429 httpdxdoiorg101098rspa19540085

Cande SC and Kent DV 1995 Revised calibration of the geomagnetic polarity timescale for the Late Cretaceous and Cenozoic Journal of Geo-physical Research Solid Earth 100(B4)6093ndash6095 httpdxdoiorg10102994JB03098

Cas RAF and Wright JV 1987 Volcanic Successions Modern and Ancient a Geological Approach to Processes Products and Successions London (Allen and Unwin)

Chaisson WP and Pearson PN 1997 Planktonic foraminifer biostratigra-phy at Site 925 middle MiocenendashPleistocene In Shackleton NJ Curry WB Richter C and Bralower TJ (Eds) Proceedings of the Ocean Drill-ing Program Scientific Results 154 College Station TX (Ocean Drilling Program) 3ndash31 httpdxdoiorg102973odpprocsr1541041997

Dunlop DJ 2003 Stepwise and continuous low-temperature demagnetiza-tion Geophysical Research Letters 30(11)1582 httpdxdoiorg1010292003GL017268

Dunlop DJ Oumlzdemir Ouml and Schmidt PW 1997 Paleomagnetism and paleothermometry of the Sydney Basin 2 Origin of anomalously high unblocking temperatures Journal of Geophysical Research Solid Earth 102(B12)27285ndash27295 httpdxdoiorg10102997JB02478

Ellis DV and Singer JM 2007 Well Logging for Earth Scientists (2nd ed) New York (Elsevier)

Evans HB 1965 GRAPEmdasha device for continuous determination of mate-rial density and porosity Transactions of the SPWLA Annual Logging Symposium 6(2)B1ndashB25 httpswwwspwlaorgSymposiumTrans-actionsgrape-device-continuous-determination-material-density-and-porosity

Expedition 304305 Scientists 2006 Methods In Blackman DK Ildefonse B John BE Ohara Y Miller DJ MacLeod CJ and the Expedition 304305 Scientists Proceedings of the Integrated Ocean Drilling Program 304305 College Station TX (Integrated Ocean Drilling Program Man-agement International Inc) httpdxdoiorg102204iodpproc3043051022006

Expedition 323 Scientists 2011 Methods In Takahashi K Ravelo AC Alvarez Zarikian CA and the Expedition 323 Scientists Proceedings of the Integrated Ocean Drilling Program 323 Tokyo (Integrated Ocean Drilling Program Management International Inc) httpdxdoiorg102204iodpproc3231022011

Expedition 324 Scientists 2010 Methods In Sager WW Sano T Geld-macher J and the Expedition 324 Scientists Proceedings of the Integrated Ocean Drilling Program 324 Tokyo (Integrated Ocean Drilling Program Management International Inc) httpdxdoiorg102204iodpproc3241022010

Expedition 330 Scientists 2012 Methods In Koppers AAP Yamazaki T Geldmacher J and the Expedition 330 Scientists Proceedings of the Inte-grated Ocean Drilling Program 330 Tokyo (Integrated Ocean Drilling Program Management International Inc) httpdxdoiorg102204iodpproc3301022012

Expedition 336 Scientists 2012 Methods In Edwards KJ Bach W Klaus A and the Expedition 336 Scientists Proceedings of the Integrated Ocean Drilling Program 336 Tokyo (Integrated Ocean Drilling Program Man-agement International Inc) httpdxdoiorg102204iodpproc3361022012

Expedition 340 Scientists 2013 Methods In Le Friant A Ishizuka O Stroncik NA and the Expedition 340 Scientists Proceedings of the Inte-grated Ocean Drilling Program 340 Tokyo (Integrated Ocean Drilling Program Management International Inc) httpdxdoiorg102204iodpproc3401022013

Fisher RV 1961 Proposed classification of volcaniclastic sediments and rocks Geological Society of America Bulletin 72(9)1409ndash1414 httpdxdoiorg1011300016-7606(1961)72[1409PCOVSA]20CO2

Fisher RV and Schmincke H-U 1984 Pyroclastic Rocks Berlin (Springer-Verlag) httpdxdoiorg101007978-3-642-74864-6

Gaacutesquez JA Perino E Marchevsky E Olsina R and Riveros A 1997 Correction of line interference in X-ray fluorescence trace analysis Appli-cation to yttrium determination in silicate rocks X-Ray Spectrometry 26(5)272ndash274

Gieskes JM Gamo T and Brumsack H 1991 Chemical methods for inter-stitial water analysis aboard JOIDES Resolution Ocean Drilling Program Technical Note 15 httpdxdoiorg102973odptn151991

Goldberg D 1997 The role of downhole measurements in marine geology and geophysics Reviews of Geophysics 35(3)315ndash342 httpdxdoiorg10102997RG00221

Govindaraju K 1989 1989 compilation of working values and sample description for 272 geostandards Geostandards Newsletter 13(S1) httpdxdoiorg101111j1751-908X1989tb00476x

Govindaraju K 1994 1994 compilation of working values and sample description for 383 geostandards Geostandards Newsletter 18(1) httpdxdoiorg101111j1751-908X1994tb00502x

Gradstein FM Ogg JG Schmitz MD and Ogg GM (Eds) 2012 The Geological Time Scale 2012 Amsterdam (Elsevier)

Harris RN Sakaguchi A Petronotis K Baxter AT Berg R Burkett A Charpentier D Choi J Diz Ferreiro P Hamahashi M Hashimoto Y Heydolph K Jovane L Kastner M Kurz W Kutterolf SO Li Y Malinverno A Martin KM Millan C Nascimento DB Saito S San-doval Gutierrez MI Screaton EJ Smith-Duque CE Solomon EA Straub SM Tanikawa W Torres ME Uchimura H Vannucchi P Yamamoto Y Yan Q and Zhao X 2013 Methods In Harris RN Sakaguchi A Petronotis K and the Expedition 344 Scientists Proceed-ings of the Integrated Ocean Drilling Program 344 College Station TX (Integrated Ocean Drilling Program) httpdxdoiorg102204iodpproc3441022013

Hermann Y 1992 Eocene through Quaternary planktonic foraminifers from the northwest Pacific Leg 126 In Taylor B Fujioka K et al Proceedings of the Ocean Drilling Program Scientific Results 126 College Station TX (Ocean Drilling Program) 271ndash284 httpdxdoiorg102973odpprocsr1261331992

Horai K and Von Herzen RP 1985 Measurement of heat flow on Leg 86 of the Deep Sea Drilling Project In Heath GR Burckle LH et al Initial Reports of the Deep Sea Drilling Project 86 Washington DC (US Gov-ernment Printing Office) 759ndash777 httpdxdoiorg102973dsdpproc861351985

Ingram RL 1954 Terminology for the thickness of stratification and parting units in sedimentary rocks Geological Society of America Bulletin 65(9)937ndash938 httpdxdoiorg1011300016-7606(1954)65[937TFT-TOS]20CO2

Jackson M Gruber W Marvin J and Banerjee SK 1988 Partial anhyster-etic remanence and its anisotropy applications and grainsize-depen-



dence Geophysical Research Letters 15(5)440ndash443 httpdxdoiorg101029GL015i005p00440

Jutzeler M White JDL Talling PJ McCanta M Morgan S Le Friant A and Ishizuka O 2014 Coring disturbances in IODP piston cores with implications for offshore record of volcanic events and the Missoula megafloods Geochemistry Geophysics Geosystems 15(9)3572ndash3590 httpdxdoiorg1010022014GC005447

Kaiho K 1992 Eocene to Quaternary benthic foraminifers and paleobathy-metry of the Izu-Bonin arc Legs 125 and 126 In Taylor B Fujioka K et al Proceedings of the Ocean Drilling Program Scientific Results 126 Col-lege Station TX (Ocean Drilling Program) 285ndash310 httpdxdoiorg102973odpprocsr1261371992

Kvenvolden KA and McDonald TJ 1986 Organic geochemistry on the JOIDES Resolutionmdashan assay Ocean Drilling Program Technical Note 6 College Station TX (Ocean Drilling Program) httpdxdoiorg102973odptn61986

Le Maitre RW Steckeisen A Zanettin B Le Bas MJ Bonin B and Bateman P (Eds) 2002 Igneous rocks A Classification and Glossary of Terms (2nd ed) Cambridge UK (Cambridge University Press)

Li B 1997 Paleoceanography of the Nansha Area southern South China Sea since the last 700000 years [PhD dissert] Nanjing Institute of Geology and Paleontology Academic Sinica Nanjing China (in Chinese with abstract in English)

Lofgren G 1974 An experimental study of plagioclase crystal morphology isothermal crystallization American Journal of Science 274243ndash273

Lourens LJ Hilgen FJ Laskar J Shackleton NJ and Wilson D 2004 The Neogene period In Gradstein FM Ogg J et al (Eds) A Geologic Time Scale 2004 Cambridge UK (Cambridge University Press) 409ndash440

Lovell MA Harvey PK Brewer TS Williams C Jackson PD and Wil-liamson G 1998 Application of FMS images in the Ocean Drilling Pro-gram an overview In Cramp A MacLeod CJ Lee SV and Jones EJW (Eds) Geological Evolution of Ocean Basins Results from the Ocean Drilling Program Geological Society Special Publication 131(1)287ndash303 httpdxdoiorg101144GSLSP19981310118

Lund SP Stoner JS Mix AC Tiedemann R Blum P and the Leg 202 Shipboard Scientific Party 2003 Appendix observations on the effect of a nonmagnetic core barrel on shipboard paleomagnetic data results from ODP Leg 202 In Mix AC Tiedemann R Blum P et al Proceedings of the Ocean Drilling Program Initial Reports 202 College Station TX (Ocean Drilling Program) 1ndash10 httpdxdoiorg102973odpprocir2021142003

MacKenzie WS Donaldson CH and Guilford C 1982 Atlas of Igneous Rocks and Their Textures Essex UK (Longman Group UK Limited)

Manheim FT and Sayles FL 1974 Composition and origin of interstitial waters of marine sediments based on deep sea drill cores In Goldberg ED (Ed) The Sea (Vol 5) Marine Chemistry The Sedimentary Cycle New York (Wiley) 527ndash568

Martini E 1971 Standard Tertiary and Quaternary calcareous nannoplank-ton zonation In Farinacci A (Ed) Proceedings of the Second Planktonic Conference Roma 1970 Rome (Edizioni Tecnoscienza) 2739ndash785

McPhie J Doyle M and Allen R 1993 Volcanic Textures A Guide to the Interpretation of Textures in Volcanic Rocks Hobart (Tasmanian Govern-ment Printing Office)

Millero FJ Feistel R Wright DG and McDougall TJ 2008 The composi-tion of Standard Seawater and the definition of the reference-composition salinity scale Deep-Sea Research Part I 55(1)50ndash72 httpdxdoiorg101016jdsr200710001

Murray RW Miller DJ and Kryc KA 2000 Analysis of major and trace elements in rocks sediments and interstitial waters by inductively cou-pled plasmandashatomic emission spectrometry (ICP-AES) Ocean Drilling Program Technical Note 29 httpdxdoiorg102973odptn292000

Musgrave RJ Collombat H and Didenko AN 1995 Magnetic sulfide dia-genesis thermal overprinting and paleomagnetism of accretionary wedge and convergent margin sediments from the Chile triple junction region In Lewis SD Behrmann JH Musgrave RJ and Cande SC (Eds) Proceedings of the Ocean Drilling Program Scientific Results 141

College Station TX (Ocean Drilling Program) 59ndash76 httpdxdoiorg102973odpprocsr1410151995

Neacuteel L 1949 Theacuteorie du traicircnage magneacutetique des ferromagneacutetiques en grains fins avec applications aux terres cuites Annales de Geophysique (Centre National de la Recherche Scientifique) 599ndash136

Okada H and Bukry D 1980 Supplementary modification and introduc-tion of code numbers to the low-latitude coccolith biostratigraphic zona-tion (Bukry 1973 1975) Marine Micropaleontology 5321ndash325 httpdxdoiorg1010160377-8398(80)90016-X

Piper DJW 1975 Deformation of stiff and semilithified cores from Legs 18 and 28 Initial Reports of the Deep Sea Drilling Project 28 Washington DC (US Government Printing Office) 977ndash979 httpdxdoiorg102973dsdpproc28app21975

Pribnow D Kinoshita M and Stein C 2000 Thermal Data Collection and Heat Flow Recalculations for Ocean Drilling Program Legs 101ndash180 Hanover Germany (Institute for Joint Geoscientific Research Institut fuumlr Geowissenschaftliche Gemeinschaftsaufgaben [GGA]) httpwww-odptamuedupublicationsheatflowODPReprtpdf

Raffi I Backman J Fornaciari E Paumllike H Rio D Lourens L and Hilgen F 2006 A review of calcareous nannofossil astrobiochronology encom-passing the past 25 million years Quaternary Science Reviews 25(23ndash24)3113ndash3137 httpdxdoiorg101016jquascirev200607007

Raffi I Backman J Rio D and Shackleton NJ 1993 PliondashPleistocene nan-nofossil biostratigraphy and calibration to oxygen isotope stratigraphies from Deep Sea Drilling Project Site 607 and Ocean Drilling Program Site 677 Paleoceanography 8(3)387ndash408 httpdxdoiorg10102993PA00755

Richter C Acton G Endris C and Radsted M 2007 Handbook for ship-board paleomagnetists Ocean Drilling Program Technical Note 34 httpdxdoiorg102973odptn342007

Rider MH 1996 The Geological Interpretation of Well Logs (2nd ed) Caith-ness Scotland (Whittles Publishing)

Roberts AP and Turner GM 1993 Diagenetic formation of ferrimagnetic iron sulphide minerals in rapidly deposited marine sediments South Island New Zealand Earth and Planetary Science Letters 115(1ndash4)257ndash273 httpdxdoiorg1010160012-821X(93)90226-Y

Schlumberger 1989 Log Interpretation PrinciplesApplications Houston (Schlumberger Education Services) SMPndash7017

Serra O 1984 Fundamentals of Well-Log Interpretation (Vol 1) The Acqui-sition of Logging Data Amsterdam (Elsevier)

Serra O 1986 Fundamentals of Well-Log Interpretation (Vol 2) The Inter-pretation of Logging Data Amsterdam (Elsevier)

Serra O 1989 Formation MicroScanner Image Interpretation Houston (Schlumberger Education Services) SMP-7028

Shipboard Scientific Party 2003 Explanatory notes In Wilson DS Teagle DAH Acton GD et al Proceedings of the Ocean Drilling Program Ini-tial Reports 206 College Station TX (Ocean Drilling Program) 1ndash94 httpdxdoiorg102973odpprocir2061022003

Stokking L Musgrave R Bontempo D Autio W Rabinowitz PD Bal-dauf J and Francis TJG 1993 Handbook for shipboard paleomagne-tists Ocean Drilling Program Technical Note 18 httpdxdoiorg102973odptn181993

Summerhayes CP and Thorpe SA 1996 Oceanography An Illustrated Guide Hoboken NJ (John Wiley amp Sons) 165ndash181

Tamura Y Busby CJ Blum P Guegraverin G Andrews GDM Barker AK Berger JLR Bongiolo EM Bordiga M DeBari SM Gill JB Hamelin C Jia J John EH Jonas A-S Jutzeler M Kars MAC Kita ZA Konrad K Mahoney SH Martini M Miyazaki T Mus-grave RJ Nascimento DB Nichols ARL Ribeiro JM Sato T Schindlbeck JC Schmitt AK Straub SM Vautravers MJ and Yang Y 2015 Site U1437 In Tamura Y Busby CJ Blum P and the Expedi-tion 350 Scientists Proceedings of the International Ocean Discovery Pro-gram Expedition 350 Izu-Bonin-Mariana Rear Arc College Station TX (International Ocean Discovery Program) httpdxdoiorg1014379iodpproc3501042015



Vasiliev MA Blum P Chubarian G Olsen R Bennight C Cobine T Fackler D Hastedt M Houpt D Mateo Z and Vasilieva YB 2011 A new natural gamma radiation measurement system for marine sediment and rock analysis Journal of Applied Geophysics 75455ndash463 httpdxdoiorg101016jjappgeo201108008

Wade BS Pearson PN Berggren WA and Paumllike H 2011 Review and revision of Cenozoic tropical planktonic foraminiferal biostratigraphy and calibration to the geomagnetic polarity and astronomical time scale Earth-Science Reviews 104(1ndash3)111ndash142 httpdxdoiorg101016jearscirev201009003

Walz F 2002 The Verwey transitionmdasha topical review Journal of Physics Condensed Matter 14(12)R285ndashR340 httpdxdoiorg1010880953-89841412203

Wentworth CK 1922 A scale of grade and class terms for clastic sediments Journal of Geology 30(5)377ndash392 httpdxdoiorg101086622910

White JDL and Houghton BF 2006 Primary volcaniclastic rocks Geology 34(8)677ndash680 httpdxdoiorg101130G223461

Zijderveld JDA 1967 AC demagnetization of rocks analysis of results In Collinson DW Creer KM and Runcorn SK (Eds) Methods in Palae-omagnetism Amsterdam (Elsevier) 254ndash286

Zurfluh FJ Hofmann BA Gnos E and Eggenberger U 2011 Evaluation of the utility of handheld XRF in meteoritics X-Ray Spectrometry 40(6)449ndash463 httpdxdoiorg101002xrs1369


Expedition 350 methods

Y Tamura CJ Busby P Blum G Guegraverin GDM Andrews AK Barker JLR Berger EM Bongiolo M Bordiga SM DeBari JB Gill C Hamelin J Jia EH John A-S Jonas M Jutzeler MAC Kars ZA Kita K Konrad SH Mahoney M Ma

Introduction

Operations

Site locations

Coring and drilling operations

Drilling disturbance

Core handling and analysis

Sample depth calculations

Shipboard core analysis

Lithostratigraphy

Lithologic description

IODP use of DESClogik

Core disturbances

Sediments and sedimentary rocks

Rationale

Description workflow

Units

Descriptive scheme for sediment and sedimentary rocks

Summary

Igneous rocks

Units

Volcanic rocks

Plutonic rocks

Textures

Alteration

Macroscopic core description

Microscopic description

VCD standard graphic summary reports

Geochemistry

Headspace analysis of hydrocarbon gases

Pore fluid analysis

Pore fluid collection

Shipboard pore fluid analyses

Sediment bulk geochemistry



ICP-AES

Sample preparation

Analysis and data reduction

Physical properties

Gamma ray attenuation bulk density

Magnetic susceptibility

P-wave velocity

Natural gamma radiation

Thermal conductivity

Moisture and density

Sediment strength

Color reflectance

Paleomagnetism

Samples instruments and measurements

Archive section half measurements

Discrete samples

Remanence measurements

Sample sharing with physical properties

Liquid nitrogen treatment

Rock-magnetic analysis

Anisotropy of magnetic susceptibility

Sample coordinates

Core orientation

Magnetostratigraphy

Biostratigraphy

Paleontology and biostratigraphy

Foraminifers

Calcareous nannofossils

Age model

Timescale

Depth scale

Constructing the age-depth model

Linear sedimentation rates

Mass accumulation rates

Downhole measurements

Wireline logging

Operations

Logged properties and tool measurement principles

Auxiliary logging equipment

Log data quality

Wireline heave compensator

Logging data flow and processing

In situ temperature measurements

References

Figures

Figure F1 New sedimentary and volcaniclastic lithology naming conventions based on relative abundances of grain and clast types Principal lithology names are compulsory for all intervals Prefixes are optional except for tuffaceous lithologies Suf

Figure F2 Visual interpretation of core disturbances in semilithified and lithified rocks in 350-U1437B-43X-1A 50ndash128 cm (left) and 350-U1437D-12R- 6A 34ndash112 cm (right)

Figure F3 Ternary diagram of volcaniclastic grain size terms and their associated sediment and rock types (modified from Fisher and Schmincke 1984)


Figure F5 A Tuff composed of glass shards and crystals described as sediment in DESClogik (350-U1437D-38R-2 TS20) B Lapilli-tuff containing pumice clasts in a glass and crystal matrix (29R TS10) The matrix and clasts are described as sediment

Figure F6 Classification of plutonic rocks following Le Maitre et al (2002) A Q-A-P diagram for leucocratic rocks B Plagioclase-clinopyroxene-orthopyroxene triangular plots and olivine-pyroxenes-plagioclase triangle for melanocratic rocks

Figure F7 Classification of vesicle sphericity and roundness (adapted from the Wentworth [1922] classification scheme for sediment grains)




Figure F11 Working curve for shipboard pXRF analysis of Y Standards include JB-2 JB-3 BHVO-2 BCR-2 AGV-1 JA-2 JR-1 JR-2 and JG-2 with Y abundances between 183 and 865 ppm Intensities of Y Kα were peak- stripped for Rb Kβ using the appr

Figure F12 Reproducibility of shipboard pXRF analysis of JB-2 powder over an ~7 week period in 2014 Errors are reported as 1σ equivalent to the observed standard deviation

Figure F13 Accuracy of shipboard pXRF analyses relative to international geochemical rock standards (solid circles Govindaraju 1994) and shipboard ICP-AES analyses of samples collected and analyzed during Expedition 350

Figure F14 A Paleomagnetic sample coordinate systems B SRM coordinate system on the JOIDES Resolution (after Harris et al 2013)

Figure F15 Scheme adopted to calculate the mean depth for foraminifer and nannofossil bioevents

Figure F16 Expedition 350 timescale based on calcareous nannofossil and planktonic foraminifer zones and datums B = bottom T = top Bc = bottom common Tc = top common Bd = bottom dominance Td = top dominance Ba = bottom acme Ta = top acme X




Figure F17 Wireline tool strings Expedition 350 See Table T15 for tool acronyms Height from the bottom is in meters VSI = Versatile Seismic Imager

Tables

Table T1 Definition of lithostratigraphic and lithologic units descriptive intervals and domains

Table T2 Relative abundances of volcanogenic material

Table T3 Particle size nomenclature and classifications

Table T4 Bed thickness classifications

Table T5 Macrofossil abundance classifications

Table T6 Explanation of nomenclature for extrusive and hypabyssal volcanic rocks

Table T7 Primary secondary and tertiary wavelengths used for rock and interstitial water measurements by ICP-AES Expedition 350

Table T8 Values for standards measured by pXRF (averages) and true (references) values

Table T9 Selected sequence of analyses in ICP-AES run Expedition 350

Table T10 JB-2 check standard major and trace element data for ICP-AES analysis Expedition 350

Table T11 Age estimates for timescale of magnetostratigraphic chrons


Table T12 Calcareous nannofossil datum events used for age estimates



Table T13 Planktonic foraminifer datum events used for age estimates


Table T14 Downhole measurements made by wireline logging tool strings

Table T15 Acronyms and units used for downhole wireline tools data and measurements

Table of contents


vances into the formation at high speed and cuts the core with a di-ameter of 66 mm (26 inches) The driller can detect a successfulcut or ldquofull strokerdquo from the pressure gauge on the rig floor

The depth limit of the APC often referred to as APC refusal isindicated in two ways (1) the piston fails to achieve a completestroke (as determined from the pump pressure reading) because theformation is too hard or (2) excessive force (gt60000 lb ~267 kN) isrequired to pull the core barrel out of the formation When a fullstroke could not be achieved additional attempts were typicallymade The assumption is made that the barrel penetrated the for-mation by the length of core recovered (nominal recovery of~100) and the bit was advanced by that length before cutting thenext core When a full or partial stroke was achieved but excessiveforce could not retrieve the barrel the core barrel was sometimesldquodrilled overrdquo meaning after the inner core barrel was successfullyshot into the formation the drill bit was advanced to total depth tofree the APC barrel

Nonmagnetic core barrels were used during all APC deploy-ments except during the return to Site U1436 at the end of the ex-pedition when no paleomagnetic measurements were neededMost APC cores recovered during Expedition 350 were oriented us-ing the FlexIT tool (see Paleomagnetism) Formation temperaturemeasurements were made to obtain temperature gradients and heatflow estimates (see Downhole measurements)

The XCB is a rotary system with a small cutting shoe that ex-tends below the large rotary APCXCB bit The smaller bit can cut asemi-indurated core with less torque and fluid circulation than themain bit optimizing recovery The XCB cutting shoe (bit) extends~305 cm ahead of the main bit in soft sediment but retracts into themain bit when hard formations are encountered It cuts a core withnominal diameter of 587 cm (2312 inches) slightly less than the 66cm diameter of the APC cores

The RCB is the most conventional rotary coring system and issuitable for lithified rock material It cuts a core with nominal diam-eter of 587 cm just as the XCB system does RCB coring can bedone with or without the core liners used routinely with theAPCXCB soft sediment systems We chose to core without theliner in the deeper parts of Hole U1437E because core piecesseemed to get caught at the edge of the liner leading to jammingand reduced recovery

The bottom-hole assembly (BHA) is the lowermost part of thedrill string A typical APCXCB BHA consists of a drill bit (outerdiameter = 11 inches) a bit sub a seal bore drill collar a landingsaver sub a modified top sub a modified head sub a nonmagneticdrill collar (for APCXCB) a number of 8 inch (~2032 cm) drill col-lars a tapered drill collar 6 joints (two stands) of 5frac12 inch (~1397cm) drill pipe and 1 crossover sub A lockable flapper valve wasused to collect downhole logs without dropping the bit whenAPCXCB coring

A typical RCB BHA consists of a drill bit a bit sub an outer corebarrel a top sub a head sub 8 joints of 8frac14 inch drill collars a ta-pered drill collar 2 joints of standard 5frac12 inch drill pipe and a cross-over sub to the regular 5 inch drill pipe

The typical casing installation consists of 20 inch casing about25 m long attached to a reentry cone with a casing hanger that re-ceives a 16 inch casing string a few hundred meters long and finallya 10frac34 inch string of several hundred meters length Installation ofthe casing in Hole U1437E which represents a record length for theJOIDES Resolution (10856 m) is described in Operations in theSite U1437 chapter (Tamura et al 2015)

Drilling disturbanceCores may be significantly disturbed as a result of the drilling

process and contain extraneous material as a result of the coringand core handling process In formations with loose granular layers(sand ash shell hash ice-rafted debris etc) granular material fromintervals higher in the hole may settle and accumulate in the bottomof the hole as a result of drilling circulation and be sampled with thenext core The uppermost 10ndash50 cm of each core must therefore beexamined critically during description for potential ldquofall-inrdquo Com-mon coring-induced deformation includes the concave-downwardappearance of originally horizontal bedding Piston action may re-sult in fluidization (flow-in) at the bottom of or even within APCcores Retrieval of unconsolidated (APC) cores from depth to thesurface typically results to some degree in elastic rebound and gasthat is in solution at depth may become free and drive core seg-ments within the liner apart When gas content is high pressuremust be relieved for safety reasons before the cores are cut into seg-ments This is accomplished by drilling holes into the liner whichforces some sediment as well as gas out of the liner XCB coring typ-ically affects torquing of the indurated core resulting in fractureddisc-shaped pieces packed with sheared and remolded core mate-rial mixed with drill slurry resembling resembled soft cream be-tween brittle ldquobiscuitsrdquo

Drilling disturbances are described in the Lithostratigraphy sec-tions in each site chapter and are graphically indicated on thegraphic core summary reports also referred to as visual core de-scriptions (VCDs) in Core descriptions

Core handling and analysisAll APC and XCB cores and some of the RCB cores recovered

during Expedition 350 were extracted from the core barrel in plasticliners These liners were carried from the rig floor to the core pro-cessing area on the catwalk outside the Core Laboratory and cutinto ~15 m sections The exact section length was noted and laterentered into the database as ldquocreated lengthrdquo using the Sample Mas-ter application This number was used to calculate recovery Thecurated length was set equal to the created length and very rarelyhad to be modified Depth in hole calculations are based on the cu-rated length

When the core liners seemed to cause jams preventing pieces toenter the barrel liners were not used Instead the recovered corewas slid and shaken out of the barrel and carefully arrange in theorder retrieved in a prepared half-liner The core pieces were thenfilled into a full liner for the purpose of splitting We did not per-form any ldquohard rock curationrdquo whereby pieces are separated with di-viders and logged separately

Headspace samples were taken from selected section ends (typi-cally 1 per core) using a syringe for immediate hydrocarbon analysisas part of the shipboard safety and pollution prevention programSimilarly whole-round samples for interstitial water analysis andmicrobiology samples were taken immediately after the core wassectioned Core catcher samples were taken for biostratigraphicanalysis When catwalk sampling was complete liner caps (blue =top colorless = bottom) were glued with acetone onto liner sec-tions and the sections were placed in core racks in the laboratoryfor analysis

After completion of whole-round section analyses (see below)the sections were split lengthwise from bottom to top into workingand archive halves The softer cores were split with a wire and



































gt25

v

olca

nic

grai

ns a

nd c

last

s


lt25

v

olca

nic

grai

ns a

nd

clas

ts

nonv

olca

nic



grains and clasts)

Tuffaceous(25-75








jim
Highlight



















terminology


































Incr

easi

ng

bisc

uitin

g in

tens

ity

Slig

htM

oder

ate

Sev

ere

Des

troy

ed

Slig

htM

oder

ate

Sev

ere

Incr

easi

ng fr

actu

re in

tens

ity
























Volcaniccomponent





volcanic breccia














1984)






Ash tuff











conglomerate










2575

2575

7525

7525


TuffLapilli

Lapillistone

Ash-breccia

Tuff-breccia





Volcanic breccia


Lapilli2ndash64 mm

Ashlt2 mm


jim
Highlight
jim
Highlight
jim
Highlight






















Sorting

Rounding

















































A B

PumicePumice

1 mm 1 mm












Q

PA

90

60

20

5

90653510

Quartzolite

Granite

Monzogranite

Sye

nogr

anite

Quartz monozite

Syenite Monzonite

Granodiorite

Tonalite

Alka

li fe

ldsp

ar g

rani

te


A

Plagioclase


Orthopyroxene

Norite

NoriteW

ehrlite

Olivine

Clinopyroxenite

Oliv

ine

orth

opyr

oxen

ite

Har

zbur

gite

Gab

bro

Gab

bro



Lherzolite


Clinopyroxenite

Orthopyroxenite

Websterite

Gabbronorite

40

Clin

opyr

oxen

e

Anorthosite90

5

B




DioriteGabbro

Anorthosite



Olivinewebsterite




If phyric


































Sphericity

High

Moderate

Low

Elongate

Pipe

Rounded

Subrounded

Subangular

Angular

Very angular

Roundness




mio

cene

VI

1

2

3

4

5

6

7

0

100

200

300

400

500

600

700

800

900137750

137650

137550

137450

137350

137250

137150

137050

136950pumice

pumice

pumice

fiamme

pillow fragment

fiamme

fiamme

fiamme

pumicefiamme

pumice

pumice

pumice

XRF

TSBTS

MAD

HS

MAD

MAD

MAD

10-40

20-80

ReflectanceL a b


(cps)

40200

MS LoopMS Point

(SI)

20000

Age

Ship

boar

dsa

mpl

es

Sedi

men

tary

stru

ctur

es

Graphiclithology

CoreimageLi

thol

ogic

unit

Sect

ion

Core

leng

th (c

m)

Dept

h CS

F-A

(m)


Dist

urba

nce

type


Dom

inan

t vitr

ic

Grain size rankMax

Modal

1062

Gra

ding

Dom

inan

t

2nd

orde

r

3rd

orde

r

Component

Clos

ely

inte

rcal

ated






Finesand


Mud Sand Gravel

ClayClaystone

MudMudstone

100001

90002

80004

70008

60016

50031

40063

30125

20250

10500

01

-12

-24

-38

-416

-532

-664

-7128

-8256

-9512

Φmm

AshLapilli



SandSandstone

Evolved ashTuff


Bimodal ashTuff

Rhyoliteor

dacite



Mafic ashTuff

Monomicticbreccia




Evolved

Mafic


Fine ash Coarse ash

Very finesand

Mediumsand

Coarsesand

Very coarsesand

Boulder

Polymictic

Monomictic

Polymictic

Monomictic

Polymictic

Monomictic

Polymictic

Monomictic

Intermediateor

bimodal




Polymicticbreccia










Tuffaceous breccia




Disturbance type

Basal flow-in

Biscuit

Brecciated

Core extension

Fall-in

Fractured

Mid-core flow-in

Sediment flowage

Soupy

Void

Component

Lithic

Crystal

Vitric


Convolute bedded

Cross-bedded

Flame structure

Intraclast

Lenticular bedded


Stratified

Grading

Density graded

Normally graded

Reversely graded



















































0 20 40 60 80 10000

01

02

03

04

Y K

α (n

orm

aliz

ed to

Ag

Com

pton

)

Y standard (ppm)

y = 000387 times x


Oxi

de (

wt

)


Ele

men

t (p

pm)





n = 131

Y = 24 plusmn 3 ppm

03

04

05

90

95

100

105

410 417 424 51 58 515 522 5290

20

40

60

150

170

190








Ref

eren

ce


Standard

plusmn20 (rel)

000 005 010 015 020 025 030000

005

010

015

020

025

030

0 2 4 6 8 10 12 14 16 180

2

4

6

8

10

12

14

16

18

00 05 10 15 20 25 3000

05

10

15

20

25

30

Sr (ppm)

0 100 200 300 400 500 600 700 8000

100

200

300

400

500

600

700

800

CaO (wt)

0 2 4 6 8 10 12 140

2

4

6

8

10

12

14

Zn (ppm)

0 50 100 1500

50

100

150

Zr (ppm)

0 50 100 150 200 250 3000

50

100

150

200

250

300

K2O (wt)

0 1 2 3 4 500

05

10

15

20

25

30

35

40

45

50

Y (ppm)

0 10 20 30 40 50 60 700

10

20

30

40

50

60

70

pXRFICP-AES



















































q = k(dTdx)



T(t) = A1 + A2 ln(t) + A3 [ln(t)t] + (A4t)














ρwet = MwetVwet

ρdry = MsolidVwet


φ = VpwVwet

and

VR = VpwVsolid















































Working half

+x = north+y = east

Bottom

+z

+y

+xTop

Top

Upcore

Upcore

Bottom

+x+z

+y

Archive half

270deg

0deg

90deg

180deg

90deg270deg

N

E

S

W



Discrete sample

Up

Bottom Up arrow+z+y

+x

Japanese cube


A

B+z

+y

+x

+x +z

+y+z

+y

+x



















B 6252C3An2n T 6436

B 6733C3Bn T 7140

B 7212C3Br1n T 7251

B 7285C3Br2n T 7454

B 7489C4n1n T 7528

B 7642C4n2n T 7695

B 8108C4r1n T 8254

B 8300C4An T 8771

B 9105C4Ar1n T 9311

B 9426C4Ar2n T 9647

B 9721C5n1n T 9786

B 9937C5n2n T 9984

B 11056C5r1n T 11146

B 11188C5r2r-1n T 11263

B 11308C5r2n T 11592

B 11657C5An1n T 12049

B 12174C5An2n T 12272

B 12474C5Ar1n T 12735

B 12770C5Ar2n T 12829

B 12887C5AAn T 13032

B 13183

C5ABn T 13363B 13608

C5ACn T 13739B 14070

C5ADn T 14163B 14609

C5Bn1n T 14775B 14870

C5Bn2n T 15032B 15160

C5Cn1n T 15974B 16268

C4Cn2n T 16303B 16472

C5Cn3n T 16543B 16721

C5Dn T 17235B 17533

C5Dr1n T 17717B 17740

C5En T 18056B 18524

C6n T 18748B 19722

C6An1n T 20040B 20213

C6An2n T 20439B 20709

C6AAn T 21083B 21159

C6AAr1n T 21403B 21483

C6AAr2n T 21659B 21688

C6Bn1n T 21767B 21936

C6Bn1n T 21992B 22268

C6Cn1n T 22564B 22754

C6Cn2n T 22902B 23030

C6Cn3n T 23233B 23295

C7n1n T 23962B 24000

C7n2n T 24109B 24474

C7An T 24761B 24984

C81n T 25099B 25264

C82n T 25304B 25987

C9n T 26420B 27439

C10n1n T 27859B 28087

C10n2n T 28141B 28278

C11n1n T 29183




B 29477C11n2n T 29527

B 29970C12n T 30591

B 31034C13n T 33157

B 33705C15n T 34999

B 35294C16n1n T 35706

B 35892C16n2n T 36051

B 36700C17n1n T 36969

B 37753C17n2n T 37872

B 38093C17n3n T 38159

B 38333C18n1n T 38615

B 39627C18n2n T 39698

B 40145C19n T 41154

B 41390C20n T 42301

B 43432C21n T 45724

B 47349C22n T 48566

B 49344C23n1n T 50628

B 50835C23n2n T 50961

B 51833C24n1n T 52620

B 53074C24n2n T 53199

B 53274C24n3n T 53416

B 53983



















ZoneSubzone









































ZoneSubzone








ZoneSubzone





ZoneSubzone


(Ma)



























ZoneSubzone


(Ma)




























ZoneSubzone


(Ma)



T

CC n

CC n+1



B

CC n

CC n+1

1680

1685

2578

2583

+6490

6495

6500

6505



















Age

(M

a)



05

0

1

15

2

25

3

35

4

45

5

Qua

tern

ary

Plio

cene

Ple

isto

cene

Hol

Zan

clea

nP

iace

nzia

nG

elas

ian

Cal

abria

nIo

nian

Taran-tian

C3n

C2An

C2Ar

C2n

C2r

C1n

C1r



















PL1

PL2

PL3PL4

PL5

PL6

Pt1

a

b

N18 N19

N20 N21

N22



























NN12

NN13

NN14NN15

NN16

NN17

NN18

NN19

NN20

NN21

CN10

CN11

CN12

CN13

CN14

CN15

b

c

a

b

a

b

c

d

a

b

a

b

1

2

1

2

1

2

3

1

2

34

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)


Neo

gene











Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr

on




Age

(M

a)

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



55

6

65

7

75

8

85

9

95

10

105

11

115

12

125

13

135

14

Neo

gene

Mio

cene

Ser

rava

llian

Tort

onia

nM

essi

nian

C5ACn

C5ABnC5ABr

C5AAnC5AAr

C5An

C5Ar

C5n

C5r

C4An

C4Ar

C4r

C4n

C3BnC3Br

C3An

C3Ar




























M8

M9

M10

M11

M12

M13

M14

a

b

a

b

a

b

N10

N11

N12

N13

N14

N15

N16

N17





































NN5

NN6

NN7

NN8

NN9

NN10

NN11

NN12

CN4

CN5

CN6

CN7

CN8

CN9

a

b

a

b

c

d

a

1

1

2

1

2

1

2

1

2

1

2

1

2

1

2

3

3

1

2

2

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)












B Neogene








and




jim
Highlight
jim
Highlight
jim
Highlight
jim
Highlight



Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



14

145

15

155

16

165

17

175

18

185

19

195

20

205

21

215

22

225

23

Neo

gene

Mio

cene

Aqu

itani

anB

urdi

galia

nLa

nghi

an

C6Cn

C6Bn

C6Br

C6AAn

C6AAr

C6Ar

C6An

C6n

C6r

C5En

C5Er

C5Dr

C5Dn

C5Cr

C5Cn

C5Br

C5Bn

C5ADn

C5ADr


























M1

M2

M3

M4

M5

M6

M7

a

b

a

b

a

b

N4

N5

N6

N7

N8

N9

N10















NN2

NN3

NN4

NN5

CN1

CN2

CN3

CN4

ab

c

12

1

2

1

2

1

2

1

2

1

2

12

3

3

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)







C Neogene

Age

(M

a)








23

235

24

245

25

255

26

265

27

275

28

285

29

295

30

305

31

315

32

325

33

335

34

345

35

355

36

365

37

375

38

385

39

40

395

Pal

eoge

ne

Eoc

ene

Olig

ocen

e

Bar

toni

anP

riabo

nian

Rup

elia

nC

hatti

an

C18n

C17r

C17n

C16n

C16r

C15n

C15r

C13n

C13r

C12n

C12r

C11n

C11r

C10n

C10r

C9n

C9r

C8n

C8r

C7AnC7Ar

C7n

C7r

C6Cn

C6Cr


























E13

E14

E15

E16

O1

O2

O3

O4

O5

O6

O7

a

P14

P15

P16 P17

P18

P19

P20

P21

P22




























NP17

NP18

NP19-NP20

NP21

NP22

NP23

NP24

NP25

NN1

CP14

CP15

CP16

CP17

CP18

CP19

b

a

b

c

ab1

2

1

2

1

2

12

1

2

1

2

1

2

1

2

3

3

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)









D Paleogene

Age

(M

a)




















Triple combo

Caliper

HLDS(density)

EDTC(telemetry

gamma ray)

HRLA(resistivity)

3986 m

3854

3656

3299

2493

1950

1600

1372

635

407367

000

Centralizer

Knuckle joints

Cablehead

Pressurebulkhead

Centralizer

MSS(magnetic

susceptibility)

FMS-sonic


EDTC(telemetry

temperatureγ ray)

Centralizer

Cablehead

3544 m

3455

3257

2901

2673

1118

890

768

000



APS(porosity)

HNGS(spectral

gamma ray)

HNGS(spectral

gamma ray)

Centralizer

Seismic

VSISonde

Shuttle

1132 m

819

183

000

EDTC(telemetry

gamma ray)

Cablehead

Tool zero





(cm)

Vertical resolution

(cm)


(cm)















































































































































Introduction

Operations

Site locations






Lithostratigraphy



Core disturbances


Rationale


Units


Summary

Igneous rocks

Units

Volcanic rocks

Plutonic rocks

Textures

Alteration




Geochemistry


Pore fluid analysis






ICP-AES

Sample preparation


Physical properties



P-wave velocity




Sediment strength

Color reflectance

Paleomagnetism



Discrete samples






Sample coordinates

Core orientation

Magnetostratigraphy

Biostratigraphy


Foraminifers


Age model

Timescale

Depth scale





Wireline logging

Operations



Log data quality




References

Figures





















Tables




















Table of contents


































gt25

v

olca

nic

grai

ns a

nd c

last

s


lt25

v

olca

nic

grai

ns a

nd

clas

ts

nonv

olca

nic



grains and clasts)

Tuffaceous(25-75








jim
Highlight



















terminology


































Incr

easi

ng

bisc

uitin

g in

tens

ity

Slig

htM

oder

ate

Sev

ere

Des

troy

ed

Slig

htM

oder

ate

Sev

ere

Incr

easi

ng fr

actu

re in

tens

ity
























Volcaniccomponent





volcanic breccia














1984)






Ash tuff











conglomerate










2575

2575

7525

7525


TuffLapilli

Lapillistone

Ash-breccia

Tuff-breccia





Volcanic breccia


Lapilli2ndash64 mm

Ashlt2 mm


jim
Highlight
jim
Highlight
jim
Highlight






















Sorting

Rounding

















































A B

PumicePumice

1 mm 1 mm












Q

PA

90

60

20

5

90653510

Quartzolite

Granite

Monzogranite

Sye

nogr

anite

Quartz monozite

Syenite Monzonite

Granodiorite

Tonalite

Alka

li fe

ldsp

ar g

rani

te


A

Plagioclase


Orthopyroxene

Norite

NoriteW

ehrlite

Olivine

Clinopyroxenite

Oliv

ine

orth

opyr

oxen

ite

Har

zbur

gite

Gab

bro

Gab

bro



Lherzolite


Clinopyroxenite

Orthopyroxenite

Websterite

Gabbronorite

40

Clin

opyr

oxen

e

Anorthosite90

5

B




DioriteGabbro

Anorthosite



Olivinewebsterite




If phyric


































Sphericity

High

Moderate

Low

Elongate

Pipe

Rounded

Subrounded

Subangular

Angular

Very angular

Roundness




mio

cene

VI

1

2

3

4

5

6

7

0

100

200

300

400

500

600

700

800

900137750

137650

137550

137450

137350

137250

137150

137050

136950pumice

pumice

pumice

fiamme

pillow fragment

fiamme

fiamme

fiamme

pumicefiamme

pumice

pumice

pumice

XRF

TSBTS

MAD

HS

MAD

MAD

MAD

10-40

20-80

ReflectanceL a b


(cps)

40200

MS LoopMS Point

(SI)

20000

Age

Ship

boar

dsa

mpl

es

Sedi

men

tary

stru

ctur

es

Graphiclithology

CoreimageLi

thol

ogic

unit

Sect

ion

Core

leng

th (c

m)

Dept

h CS

F-A

(m)


Dist

urba

nce

type


Dom

inan

t vitr

ic

Grain size rankMax

Modal

1062

Gra

ding

Dom

inan

t

2nd

orde

r

3rd

orde

r

Component

Clos

ely

inte

rcal

ated






Finesand


Mud Sand Gravel

ClayClaystone

MudMudstone

100001

90002

80004

70008

60016

50031

40063

30125

20250

10500

01

-12

-24

-38

-416

-532

-664

-7128

-8256

-9512

Φmm

AshLapilli



SandSandstone

Evolved ashTuff


Bimodal ashTuff

Rhyoliteor

dacite



Mafic ashTuff

Monomicticbreccia




Evolved

Mafic


Fine ash Coarse ash

Very finesand

Mediumsand

Coarsesand

Very coarsesand

Boulder

Polymictic

Monomictic

Polymictic

Monomictic

Polymictic

Monomictic

Polymictic

Monomictic

Intermediateor

bimodal




Polymicticbreccia










Tuffaceous breccia




Disturbance type

Basal flow-in

Biscuit

Brecciated

Core extension

Fall-in

Fractured

Mid-core flow-in

Sediment flowage

Soupy

Void

Component

Lithic

Crystal

Vitric


Convolute bedded

Cross-bedded

Flame structure

Intraclast

Lenticular bedded


Stratified

Grading

Density graded

Normally graded

Reversely graded



















































0 20 40 60 80 10000

01

02

03

04

Y K

α (n

orm

aliz

ed to

Ag

Com

pton

)

Y standard (ppm)

y = 000387 times x


Oxi

de (

wt

)


Ele

men

t (p

pm)





n = 131

Y = 24 plusmn 3 ppm

03

04

05

90

95

100

105

410 417 424 51 58 515 522 5290

20

40

60

150

170

190








Ref

eren

ce


Standard

plusmn20 (rel)

000 005 010 015 020 025 030000

005

010

015

020

025

030

0 2 4 6 8 10 12 14 16 180

2

4

6

8

10

12

14

16

18

00 05 10 15 20 25 3000

05

10

15

20

25

30

Sr (ppm)

0 100 200 300 400 500 600 700 8000

100

200

300

400

500

600

700

800

CaO (wt)

0 2 4 6 8 10 12 140

2

4

6

8

10

12

14

Zn (ppm)

0 50 100 1500

50

100

150

Zr (ppm)

0 50 100 150 200 250 3000

50

100

150

200

250

300

K2O (wt)

0 1 2 3 4 500

05

10

15

20

25

30

35

40

45

50

Y (ppm)

0 10 20 30 40 50 60 700

10

20

30

40

50

60

70

pXRFICP-AES



















































q = k(dTdx)



T(t) = A1 + A2 ln(t) + A3 [ln(t)t] + (A4t)














ρwet = MwetVwet

ρdry = MsolidVwet


φ = VpwVwet

and

VR = VpwVsolid















































Working half

+x = north+y = east

Bottom

+z

+y

+xTop

Top

Upcore

Upcore

Bottom

+x+z

+y

Archive half

270deg

0deg

90deg

180deg

90deg270deg

N

E

S

W



Discrete sample

Up

Bottom Up arrow+z+y

+x

Japanese cube


A

B+z

+y

+x

+x +z

+y+z

+y

+x



















B 6252C3An2n T 6436

B 6733C3Bn T 7140

B 7212C3Br1n T 7251

B 7285C3Br2n T 7454

B 7489C4n1n T 7528

B 7642C4n2n T 7695

B 8108C4r1n T 8254

B 8300C4An T 8771

B 9105C4Ar1n T 9311

B 9426C4Ar2n T 9647

B 9721C5n1n T 9786

B 9937C5n2n T 9984

B 11056C5r1n T 11146

B 11188C5r2r-1n T 11263

B 11308C5r2n T 11592

B 11657C5An1n T 12049

B 12174C5An2n T 12272

B 12474C5Ar1n T 12735

B 12770C5Ar2n T 12829

B 12887C5AAn T 13032

B 13183

C5ABn T 13363B 13608

C5ACn T 13739B 14070

C5ADn T 14163B 14609

C5Bn1n T 14775B 14870

C5Bn2n T 15032B 15160

C5Cn1n T 15974B 16268

C4Cn2n T 16303B 16472

C5Cn3n T 16543B 16721

C5Dn T 17235B 17533

C5Dr1n T 17717B 17740

C5En T 18056B 18524

C6n T 18748B 19722

C6An1n T 20040B 20213

C6An2n T 20439B 20709

C6AAn T 21083B 21159

C6AAr1n T 21403B 21483

C6AAr2n T 21659B 21688

C6Bn1n T 21767B 21936

C6Bn1n T 21992B 22268

C6Cn1n T 22564B 22754

C6Cn2n T 22902B 23030

C6Cn3n T 23233B 23295

C7n1n T 23962B 24000

C7n2n T 24109B 24474

C7An T 24761B 24984

C81n T 25099B 25264

C82n T 25304B 25987

C9n T 26420B 27439

C10n1n T 27859B 28087

C10n2n T 28141B 28278

C11n1n T 29183




B 29477C11n2n T 29527

B 29970C12n T 30591

B 31034C13n T 33157

B 33705C15n T 34999

B 35294C16n1n T 35706

B 35892C16n2n T 36051

B 36700C17n1n T 36969

B 37753C17n2n T 37872

B 38093C17n3n T 38159

B 38333C18n1n T 38615

B 39627C18n2n T 39698

B 40145C19n T 41154

B 41390C20n T 42301

B 43432C21n T 45724

B 47349C22n T 48566

B 49344C23n1n T 50628

B 50835C23n2n T 50961

B 51833C24n1n T 52620

B 53074C24n2n T 53199

B 53274C24n3n T 53416

B 53983



















ZoneSubzone









































ZoneSubzone








ZoneSubzone





ZoneSubzone


(Ma)



























ZoneSubzone


(Ma)




























ZoneSubzone


(Ma)



T

CC n

CC n+1



B

CC n

CC n+1

1680

1685

2578

2583

+6490

6495

6500

6505



















Age

(M

a)



05

0

1

15

2

25

3

35

4

45

5

Qua

tern

ary

Plio

cene

Ple

isto

cene

Hol

Zan

clea

nP

iace

nzia

nG

elas

ian

Cal

abria

nIo

nian

Taran-tian

C3n

C2An

C2Ar

C2n

C2r

C1n

C1r



















PL1

PL2

PL3PL4

PL5

PL6

Pt1

a

b

N18 N19

N20 N21

N22



























NN12

NN13

NN14NN15

NN16

NN17

NN18

NN19

NN20

NN21

CN10

CN11

CN12

CN13

CN14

CN15

b

c

a

b

a

b

c

d

a

b

a

b

1

2

1

2

1

2

3

1

2

34

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)


Neo

gene











Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr

on




Age

(M

a)

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



55

6

65

7

75

8

85

9

95

10

105

11

115

12

125

13

135

14

Neo

gene

Mio

cene

Ser

rava

llian

Tort

onia

nM

essi

nian

C5ACn

C5ABnC5ABr

C5AAnC5AAr

C5An

C5Ar

C5n

C5r

C4An

C4Ar

C4r

C4n

C3BnC3Br

C3An

C3Ar




























M8

M9

M10

M11

M12

M13

M14

a

b

a

b

a

b

N10

N11

N12

N13

N14

N15

N16

N17





































NN5

NN6

NN7

NN8

NN9

NN10

NN11

NN12

CN4

CN5

CN6

CN7

CN8

CN9

a

b

a

b

c

d

a

1

1

2

1

2

1

2

1

2

1

2

1

2

1

2

3

3

1

2

2

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)












B Neogene








and




jim
Highlight
jim
Highlight
jim
Highlight
jim
Highlight



Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



14

145

15

155

16

165

17

175

18

185

19

195

20

205

21

215

22

225

23

Neo

gene

Mio

cene

Aqu

itani

anB

urdi

galia

nLa

nghi

an

C6Cn

C6Bn

C6Br

C6AAn

C6AAr

C6Ar

C6An

C6n

C6r

C5En

C5Er

C5Dr

C5Dn

C5Cr

C5Cn

C5Br

C5Bn

C5ADn

C5ADr


























M1

M2

M3

M4

M5

M6

M7

a

b

a

b

a

b

N4

N5

N6

N7

N8

N9

N10















NN2

NN3

NN4

NN5

CN1

CN2

CN3

CN4

ab

c

12

1

2

1

2

1

2

1

2

1

2

12

3

3

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)







C Neogene

Age

(M

a)








23

235

24

245

25

255

26

265

27

275

28

285

29

295

30

305

31

315

32

325

33

335

34

345

35

355

36

365

37

375

38

385

39

40

395

Pal

eoge

ne

Eoc

ene

Olig

ocen

e

Bar

toni

anP

riabo

nian

Rup

elia

nC

hatti

an

C18n

C17r

C17n

C16n

C16r

C15n

C15r

C13n

C13r

C12n

C12r

C11n

C11r

C10n

C10r

C9n

C9r

C8n

C8r

C7AnC7Ar

C7n

C7r

C6Cn

C6Cr


























E13

E14

E15

E16

O1

O2

O3

O4

O5

O6

O7

a

P14

P15

P16 P17

P18

P19

P20

P21

P22




























NP17

NP18

NP19-NP20

NP21

NP22

NP23

NP24

NP25

NN1

CP14

CP15

CP16

CP17

CP18

CP19

b

a

b

c

ab1

2

1

2

1

2

12

1

2

1

2

1

2

1

2

3

3

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)









D Paleogene

Age

(M

a)




















Triple combo

Caliper

HLDS(density)

EDTC(telemetry

gamma ray)

HRLA(resistivity)

3986 m

3854

3656

3299

2493

1950

1600

1372

635

407367

000

Centralizer

Knuckle joints

Cablehead

Pressurebulkhead

Centralizer

MSS(magnetic

susceptibility)

FMS-sonic


EDTC(telemetry

temperatureγ ray)

Centralizer

Cablehead

3544 m

3455

3257

2901

2673

1118

890

768

000



APS(porosity)

HNGS(spectral

gamma ray)

HNGS(spectral

gamma ray)

Centralizer

Seismic

VSISonde

Shuttle

1132 m

819

183

000

EDTC(telemetry

gamma ray)

Cablehead

Tool zero





(cm)

Vertical resolution

(cm)


(cm)















































































































































Introduction

Operations

Site locations






Lithostratigraphy



Core disturbances


Rationale


Units


Summary

Igneous rocks

Units

Volcanic rocks

Plutonic rocks

Textures

Alteration




Geochemistry


Pore fluid analysis






ICP-AES

Sample preparation


Physical properties



P-wave velocity




Sediment strength

Color reflectance

Paleomagnetism



Discrete samples






Sample coordinates

Core orientation

Magnetostratigraphy

Biostratigraphy


Foraminifers


Age model

Timescale

Depth scale





Wireline logging

Operations



Log data quality




References

Figures





















Tables




















Table of contents



















terminology


































Incr

easi

ng

bisc

uitin

g in

tens

ity

Slig

htM

oder

ate

Sev

ere

Des

troy

ed

Slig

htM

oder

ate

Sev

ere

Incr

easi

ng fr

actu

re in

tens

ity
























Volcaniccomponent





volcanic breccia














1984)






Ash tuff











conglomerate










2575

2575

7525

7525


TuffLapilli

Lapillistone

Ash-breccia

Tuff-breccia





Volcanic breccia


Lapilli2ndash64 mm

Ashlt2 mm


jim
Highlight
jim
Highlight
jim
Highlight






















Sorting

Rounding

















































A B

PumicePumice

1 mm 1 mm












Q

PA

90

60

20

5

90653510

Quartzolite

Granite

Monzogranite

Sye

nogr

anite

Quartz monozite

Syenite Monzonite

Granodiorite

Tonalite

Alka

li fe

ldsp

ar g

rani

te


A

Plagioclase


Orthopyroxene

Norite

NoriteW

ehrlite

Olivine

Clinopyroxenite

Oliv

ine

orth

opyr

oxen

ite

Har

zbur

gite

Gab

bro

Gab

bro



Lherzolite


Clinopyroxenite

Orthopyroxenite

Websterite

Gabbronorite

40

Clin

opyr

oxen

e

Anorthosite90

5

B




DioriteGabbro

Anorthosite



Olivinewebsterite




If phyric


































Sphericity

High

Moderate

Low

Elongate

Pipe

Rounded

Subrounded

Subangular

Angular

Very angular

Roundness




mio

cene

VI

1

2

3

4

5

6

7

0

100

200

300

400

500

600

700

800

900137750

137650

137550

137450

137350

137250

137150

137050

136950pumice

pumice

pumice

fiamme

pillow fragment

fiamme

fiamme

fiamme

pumicefiamme

pumice

pumice

pumice

XRF

TSBTS

MAD

HS

MAD

MAD

MAD

10-40

20-80

ReflectanceL a b


(cps)

40200

MS LoopMS Point

(SI)

20000

Age

Ship

boar

dsa

mpl

es

Sedi

men

tary

stru

ctur

es

Graphiclithology

CoreimageLi

thol

ogic

unit

Sect

ion

Core

leng

th (c

m)

Dept

h CS

F-A

(m)


Dist

urba

nce

type


Dom

inan

t vitr

ic

Grain size rankMax

Modal

1062

Gra

ding

Dom

inan

t

2nd

orde

r

3rd

orde

r

Component

Clos

ely

inte

rcal

ated






Finesand


Mud Sand Gravel

ClayClaystone

MudMudstone

100001

90002

80004

70008

60016

50031

40063

30125

20250

10500

01

-12

-24

-38

-416

-532

-664

-7128

-8256

-9512

Φmm

AshLapilli



SandSandstone

Evolved ashTuff


Bimodal ashTuff

Rhyoliteor

dacite



Mafic ashTuff

Monomicticbreccia




Evolved

Mafic


Fine ash Coarse ash

Very finesand

Mediumsand

Coarsesand

Very coarsesand

Boulder

Polymictic

Monomictic

Polymictic

Monomictic

Polymictic

Monomictic

Polymictic

Monomictic

Intermediateor

bimodal




Polymicticbreccia










Tuffaceous breccia




Disturbance type

Basal flow-in

Biscuit

Brecciated

Core extension

Fall-in

Fractured

Mid-core flow-in

Sediment flowage

Soupy

Void

Component

Lithic

Crystal

Vitric


Convolute bedded

Cross-bedded

Flame structure

Intraclast

Lenticular bedded


Stratified

Grading

Density graded

Normally graded

Reversely graded



















































0 20 40 60 80 10000

01

02

03

04

Y K

α (n

orm

aliz

ed to

Ag

Com

pton

)

Y standard (ppm)

y = 000387 times x


Oxi

de (

wt

)


Ele

men

t (p

pm)





n = 131

Y = 24 plusmn 3 ppm

03

04

05

90

95

100

105

410 417 424 51 58 515 522 5290

20

40

60

150

170

190








Ref

eren

ce


Standard

plusmn20 (rel)

000 005 010 015 020 025 030000

005

010

015

020

025

030

0 2 4 6 8 10 12 14 16 180

2

4

6

8

10

12

14

16

18

00 05 10 15 20 25 3000

05

10

15

20

25

30

Sr (ppm)

0 100 200 300 400 500 600 700 8000

100

200

300

400

500

600

700

800

CaO (wt)

0 2 4 6 8 10 12 140

2

4

6

8

10

12

14

Zn (ppm)

0 50 100 1500

50

100

150

Zr (ppm)

0 50 100 150 200 250 3000

50

100

150

200

250

300

K2O (wt)

0 1 2 3 4 500

05

10

15

20

25

30

35

40

45

50

Y (ppm)

0 10 20 30 40 50 60 700

10

20

30

40

50

60

70

pXRFICP-AES



















































q = k(dTdx)



T(t) = A1 + A2 ln(t) + A3 [ln(t)t] + (A4t)














ρwet = MwetVwet

ρdry = MsolidVwet


φ = VpwVwet

and

VR = VpwVsolid















































Working half

+x = north+y = east

Bottom

+z

+y

+xTop

Top

Upcore

Upcore

Bottom

+x+z

+y

Archive half

270deg

0deg

90deg

180deg

90deg270deg

N

E

S

W



Discrete sample

Up

Bottom Up arrow+z+y

+x

Japanese cube


A

B+z

+y

+x

+x +z

+y+z

+y

+x



















B 6252C3An2n T 6436

B 6733C3Bn T 7140

B 7212C3Br1n T 7251

B 7285C3Br2n T 7454

B 7489C4n1n T 7528

B 7642C4n2n T 7695

B 8108C4r1n T 8254

B 8300C4An T 8771

B 9105C4Ar1n T 9311

B 9426C4Ar2n T 9647

B 9721C5n1n T 9786

B 9937C5n2n T 9984

B 11056C5r1n T 11146

B 11188C5r2r-1n T 11263

B 11308C5r2n T 11592

B 11657C5An1n T 12049

B 12174C5An2n T 12272

B 12474C5Ar1n T 12735

B 12770C5Ar2n T 12829

B 12887C5AAn T 13032

B 13183

C5ABn T 13363B 13608

C5ACn T 13739B 14070

C5ADn T 14163B 14609

C5Bn1n T 14775B 14870

C5Bn2n T 15032B 15160

C5Cn1n T 15974B 16268

C4Cn2n T 16303B 16472

C5Cn3n T 16543B 16721

C5Dn T 17235B 17533

C5Dr1n T 17717B 17740

C5En T 18056B 18524

C6n T 18748B 19722

C6An1n T 20040B 20213

C6An2n T 20439B 20709

C6AAn T 21083B 21159

C6AAr1n T 21403B 21483

C6AAr2n T 21659B 21688

C6Bn1n T 21767B 21936

C6Bn1n T 21992B 22268

C6Cn1n T 22564B 22754

C6Cn2n T 22902B 23030

C6Cn3n T 23233B 23295

C7n1n T 23962B 24000

C7n2n T 24109B 24474

C7An T 24761B 24984

C81n T 25099B 25264

C82n T 25304B 25987

C9n T 26420B 27439

C10n1n T 27859B 28087

C10n2n T 28141B 28278

C11n1n T 29183




B 29477C11n2n T 29527

B 29970C12n T 30591

B 31034C13n T 33157

B 33705C15n T 34999

B 35294C16n1n T 35706

B 35892C16n2n T 36051

B 36700C17n1n T 36969

B 37753C17n2n T 37872

B 38093C17n3n T 38159

B 38333C18n1n T 38615

B 39627C18n2n T 39698

B 40145C19n T 41154

B 41390C20n T 42301

B 43432C21n T 45724

B 47349C22n T 48566

B 49344C23n1n T 50628

B 50835C23n2n T 50961

B 51833C24n1n T 52620

B 53074C24n2n T 53199

B 53274C24n3n T 53416

B 53983



















ZoneSubzone









































ZoneSubzone








ZoneSubzone





ZoneSubzone


(Ma)



























ZoneSubzone


(Ma)




























ZoneSubzone


(Ma)



T

CC n

CC n+1



B

CC n

CC n+1

1680

1685

2578

2583

+6490

6495

6500

6505



















Age

(M

a)



05

0

1

15

2

25

3

35

4

45

5

Qua

tern

ary

Plio

cene

Ple

isto

cene

Hol

Zan

clea

nP

iace

nzia

nG

elas

ian

Cal

abria

nIo

nian

Taran-tian

C3n

C2An

C2Ar

C2n

C2r

C1n

C1r



















PL1

PL2

PL3PL4

PL5

PL6

Pt1

a

b

N18 N19

N20 N21

N22



























NN12

NN13

NN14NN15

NN16

NN17

NN18

NN19

NN20

NN21

CN10

CN11

CN12

CN13

CN14

CN15

b

c

a

b

a

b

c

d

a

b

a

b

1

2

1

2

1

2

3

1

2

34

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)


Neo

gene











Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr

on




Age

(M

a)

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



55

6

65

7

75

8

85

9

95

10

105

11

115

12

125

13

135

14

Neo

gene

Mio

cene

Ser

rava

llian

Tort

onia

nM

essi

nian

C5ACn

C5ABnC5ABr

C5AAnC5AAr

C5An

C5Ar

C5n

C5r

C4An

C4Ar

C4r

C4n

C3BnC3Br

C3An

C3Ar




























M8

M9

M10

M11

M12

M13

M14

a

b

a

b

a

b

N10

N11

N12

N13

N14

N15

N16

N17





































NN5

NN6

NN7

NN8

NN9

NN10

NN11

NN12

CN4

CN5

CN6

CN7

CN8

CN9

a

b

a

b

c

d

a

1

1

2

1

2

1

2

1

2

1

2

1

2

1

2

3

3

1

2

2

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)












B Neogene








and




jim
Highlight
jim
Highlight
jim
Highlight
jim
Highlight



Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



14

145

15

155

16

165

17

175

18

185

19

195

20

205

21

215

22

225

23

Neo

gene

Mio

cene

Aqu

itani

anB

urdi

galia

nLa

nghi

an

C6Cn

C6Bn

C6Br

C6AAn

C6AAr

C6Ar

C6An

C6n

C6r

C5En

C5Er

C5Dr

C5Dn

C5Cr

C5Cn

C5Br

C5Bn

C5ADn

C5ADr


























M1

M2

M3

M4

M5

M6

M7

a

b

a

b

a

b

N4

N5

N6

N7

N8

N9

N10















NN2

NN3

NN4

NN5

CN1

CN2

CN3

CN4

ab

c

12

1

2

1

2

1

2

1

2

1

2

12

3

3

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)







C Neogene

Age

(M

a)








23

235

24

245

25

255

26

265

27

275

28

285

29

295

30

305

31

315

32

325

33

335

34

345

35

355

36

365

37

375

38

385

39

40

395

Pal

eoge

ne

Eoc

ene

Olig

ocen

e

Bar

toni

anP

riabo

nian

Rup

elia

nC

hatti

an

C18n

C17r

C17n

C16n

C16r

C15n

C15r

C13n

C13r

C12n

C12r

C11n

C11r

C10n

C10r

C9n

C9r

C8n

C8r

C7AnC7Ar

C7n

C7r

C6Cn

C6Cr


























E13

E14

E15

E16

O1

O2

O3

O4

O5

O6

O7

a

P14

P15

P16 P17

P18

P19

P20

P21

P22




























NP17

NP18

NP19-NP20

NP21

NP22

NP23

NP24

NP25

NN1

CP14

CP15

CP16

CP17

CP18

CP19

b

a

b

c

ab1

2

1

2

1

2

12

1

2

1

2

1

2

1

2

3

3

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)









D Paleogene

Age

(M

a)




















Triple combo

Caliper

HLDS(density)

EDTC(telemetry

gamma ray)

HRLA(resistivity)

3986 m

3854

3656

3299

2493

1950

1600

1372

635

407367

000

Centralizer

Knuckle joints

Cablehead

Pressurebulkhead

Centralizer

MSS(magnetic

susceptibility)

FMS-sonic


EDTC(telemetry

temperatureγ ray)

Centralizer

Cablehead

3544 m

3455

3257

2901

2673

1118

890

768

000



APS(porosity)

HNGS(spectral

gamma ray)

HNGS(spectral

gamma ray)

Centralizer

Seismic

VSISonde

Shuttle

1132 m

819

183

000

EDTC(telemetry

gamma ray)

Cablehead

Tool zero





(cm)

Vertical resolution

(cm)


(cm)















































































































































Introduction

Operations

Site locations






Lithostratigraphy



Core disturbances


Rationale


Units


Summary

Igneous rocks

Units

Volcanic rocks

Plutonic rocks

Textures

Alteration




Geochemistry


Pore fluid analysis






ICP-AES

Sample preparation


Physical properties



P-wave velocity




Sediment strength

Color reflectance

Paleomagnetism



Discrete samples






Sample coordinates

Core orientation

Magnetostratigraphy

Biostratigraphy


Foraminifers


Age model

Timescale

Depth scale





Wireline logging

Operations



Log data quality




References

Figures





















Tables




















Table of contents
















Incr

easi

ng

bisc

uitin

g in

tens

ity

Slig

htM

oder

ate

Sev

ere

Des

troy

ed

Slig

htM

oder

ate

Sev

ere

Incr

easi

ng fr

actu

re in

tens

ity
























Volcaniccomponent





volcanic breccia














1984)






Ash tuff











conglomerate










2575

2575

7525

7525


TuffLapilli

Lapillistone

Ash-breccia

Tuff-breccia





Volcanic breccia


Lapilli2ndash64 mm

Ashlt2 mm


jim
Highlight
jim
Highlight
jim
Highlight






















Sorting

Rounding

















































A B

PumicePumice

1 mm 1 mm












Q

PA

90

60

20

5

90653510

Quartzolite

Granite

Monzogranite

Sye

nogr

anite

Quartz monozite

Syenite Monzonite

Granodiorite

Tonalite

Alka

li fe

ldsp

ar g

rani

te


A

Plagioclase


Orthopyroxene

Norite

NoriteW

ehrlite

Olivine

Clinopyroxenite

Oliv

ine

orth

opyr

oxen

ite

Har

zbur

gite

Gab

bro

Gab

bro



Lherzolite


Clinopyroxenite

Orthopyroxenite

Websterite

Gabbronorite

40

Clin

opyr

oxen

e

Anorthosite90

5

B




DioriteGabbro

Anorthosite



Olivinewebsterite




If phyric


































Sphericity

High

Moderate

Low

Elongate

Pipe

Rounded

Subrounded

Subangular

Angular

Very angular

Roundness




mio

cene

VI

1

2

3

4

5

6

7

0

100

200

300

400

500

600

700

800

900137750

137650

137550

137450

137350

137250

137150

137050

136950pumice

pumice

pumice

fiamme

pillow fragment

fiamme

fiamme

fiamme

pumicefiamme

pumice

pumice

pumice

XRF

TSBTS

MAD

HS

MAD

MAD

MAD

10-40

20-80

ReflectanceL a b


(cps)

40200

MS LoopMS Point

(SI)

20000

Age

Ship

boar

dsa

mpl

es

Sedi

men

tary

stru

ctur

es

Graphiclithology

CoreimageLi

thol

ogic

unit

Sect

ion

Core

leng

th (c

m)

Dept

h CS

F-A

(m)


Dist

urba

nce

type


Dom

inan

t vitr

ic

Grain size rankMax

Modal

1062

Gra

ding

Dom

inan

t

2nd

orde

r

3rd

orde

r

Component

Clos

ely

inte

rcal

ated






Finesand


Mud Sand Gravel

ClayClaystone

MudMudstone

100001

90002

80004

70008

60016

50031

40063

30125

20250

10500

01

-12

-24

-38

-416

-532

-664

-7128

-8256

-9512

Φmm

AshLapilli



SandSandstone

Evolved ashTuff


Bimodal ashTuff

Rhyoliteor

dacite



Mafic ashTuff

Monomicticbreccia




Evolved

Mafic


Fine ash Coarse ash

Very finesand

Mediumsand

Coarsesand

Very coarsesand

Boulder

Polymictic

Monomictic

Polymictic

Monomictic

Polymictic

Monomictic

Polymictic

Monomictic

Intermediateor

bimodal




Polymicticbreccia










Tuffaceous breccia




Disturbance type

Basal flow-in

Biscuit

Brecciated

Core extension

Fall-in

Fractured

Mid-core flow-in

Sediment flowage

Soupy

Void

Component

Lithic

Crystal

Vitric


Convolute bedded

Cross-bedded

Flame structure

Intraclast

Lenticular bedded


Stratified

Grading

Density graded

Normally graded

Reversely graded



















































0 20 40 60 80 10000

01

02

03

04

Y K

α (n

orm

aliz

ed to

Ag

Com

pton

)

Y standard (ppm)

y = 000387 times x


Oxi

de (

wt

)


Ele

men

t (p

pm)





n = 131

Y = 24 plusmn 3 ppm

03

04

05

90

95

100

105

410 417 424 51 58 515 522 5290

20

40

60

150

170

190








Ref

eren

ce


Standard

plusmn20 (rel)

000 005 010 015 020 025 030000

005

010

015

020

025

030

0 2 4 6 8 10 12 14 16 180

2

4

6

8

10

12

14

16

18

00 05 10 15 20 25 3000

05

10

15

20

25

30

Sr (ppm)

0 100 200 300 400 500 600 700 8000

100

200

300

400

500

600

700

800

CaO (wt)

0 2 4 6 8 10 12 140

2

4

6

8

10

12

14

Zn (ppm)

0 50 100 1500

50

100

150

Zr (ppm)

0 50 100 150 200 250 3000

50

100

150

200

250

300

K2O (wt)

0 1 2 3 4 500

05

10

15

20

25

30

35

40

45

50

Y (ppm)

0 10 20 30 40 50 60 700

10

20

30

40

50

60

70

pXRFICP-AES



















































q = k(dTdx)



T(t) = A1 + A2 ln(t) + A3 [ln(t)t] + (A4t)














ρwet = MwetVwet

ρdry = MsolidVwet


φ = VpwVwet

and

VR = VpwVsolid















































Working half

+x = north+y = east

Bottom

+z

+y

+xTop

Top

Upcore

Upcore

Bottom

+x+z

+y

Archive half

270deg

0deg

90deg

180deg

90deg270deg

N

E

S

W



Discrete sample

Up

Bottom Up arrow+z+y

+x

Japanese cube


A

B+z

+y

+x

+x +z

+y+z

+y

+x



















B 6252C3An2n T 6436

B 6733C3Bn T 7140

B 7212C3Br1n T 7251

B 7285C3Br2n T 7454

B 7489C4n1n T 7528

B 7642C4n2n T 7695

B 8108C4r1n T 8254

B 8300C4An T 8771

B 9105C4Ar1n T 9311

B 9426C4Ar2n T 9647

B 9721C5n1n T 9786

B 9937C5n2n T 9984

B 11056C5r1n T 11146

B 11188C5r2r-1n T 11263

B 11308C5r2n T 11592

B 11657C5An1n T 12049

B 12174C5An2n T 12272

B 12474C5Ar1n T 12735

B 12770C5Ar2n T 12829

B 12887C5AAn T 13032

B 13183

C5ABn T 13363B 13608

C5ACn T 13739B 14070

C5ADn T 14163B 14609

C5Bn1n T 14775B 14870

C5Bn2n T 15032B 15160

C5Cn1n T 15974B 16268

C4Cn2n T 16303B 16472

C5Cn3n T 16543B 16721

C5Dn T 17235B 17533

C5Dr1n T 17717B 17740

C5En T 18056B 18524

C6n T 18748B 19722

C6An1n T 20040B 20213

C6An2n T 20439B 20709

C6AAn T 21083B 21159

C6AAr1n T 21403B 21483

C6AAr2n T 21659B 21688

C6Bn1n T 21767B 21936

C6Bn1n T 21992B 22268

C6Cn1n T 22564B 22754

C6Cn2n T 22902B 23030

C6Cn3n T 23233B 23295

C7n1n T 23962B 24000

C7n2n T 24109B 24474

C7An T 24761B 24984

C81n T 25099B 25264

C82n T 25304B 25987

C9n T 26420B 27439

C10n1n T 27859B 28087

C10n2n T 28141B 28278

C11n1n T 29183




B 29477C11n2n T 29527

B 29970C12n T 30591

B 31034C13n T 33157

B 33705C15n T 34999

B 35294C16n1n T 35706

B 35892C16n2n T 36051

B 36700C17n1n T 36969

B 37753C17n2n T 37872

B 38093C17n3n T 38159

B 38333C18n1n T 38615

B 39627C18n2n T 39698

B 40145C19n T 41154

B 41390C20n T 42301

B 43432C21n T 45724

B 47349C22n T 48566

B 49344C23n1n T 50628

B 50835C23n2n T 50961

B 51833C24n1n T 52620

B 53074C24n2n T 53199

B 53274C24n3n T 53416

B 53983



















ZoneSubzone









































ZoneSubzone








ZoneSubzone





ZoneSubzone


(Ma)



























ZoneSubzone


(Ma)




























ZoneSubzone


(Ma)



T

CC n

CC n+1



B

CC n

CC n+1

1680

1685

2578

2583

+6490

6495

6500

6505



















Age

(M

a)



05

0

1

15

2

25

3

35

4

45

5

Qua

tern

ary

Plio

cene

Ple

isto

cene

Hol

Zan

clea

nP

iace

nzia

nG

elas

ian

Cal

abria

nIo

nian

Taran-tian

C3n

C2An

C2Ar

C2n

C2r

C1n

C1r



















PL1

PL2

PL3PL4

PL5

PL6

Pt1

a

b

N18 N19

N20 N21

N22



























NN12

NN13

NN14NN15

NN16

NN17

NN18

NN19

NN20

NN21

CN10

CN11

CN12

CN13

CN14

CN15

b

c

a

b

a

b

c

d

a

b

a

b

1

2

1

2

1

2

3

1

2

34

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)


Neo

gene











Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr

on




Age

(M

a)

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



55

6

65

7

75

8

85

9

95

10

105

11

115

12

125

13

135

14

Neo

gene

Mio

cene

Ser

rava

llian

Tort

onia

nM

essi

nian

C5ACn

C5ABnC5ABr

C5AAnC5AAr

C5An

C5Ar

C5n

C5r

C4An

C4Ar

C4r

C4n

C3BnC3Br

C3An

C3Ar




























M8

M9

M10

M11

M12

M13

M14

a

b

a

b

a

b

N10

N11

N12

N13

N14

N15

N16

N17





































NN5

NN6

NN7

NN8

NN9

NN10

NN11

NN12

CN4

CN5

CN6

CN7

CN8

CN9

a

b

a

b

c

d

a

1

1

2

1

2

1

2

1

2

1

2

1

2

1

2

3

3

1

2

2

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)












B Neogene








and




jim
Highlight
jim
Highlight
jim
Highlight
jim
Highlight



Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



14

145

15

155

16

165

17

175

18

185

19

195

20

205

21

215

22

225

23

Neo

gene

Mio

cene

Aqu

itani

anB

urdi

galia

nLa

nghi

an

C6Cn

C6Bn

C6Br

C6AAn

C6AAr

C6Ar

C6An

C6n

C6r

C5En

C5Er

C5Dr

C5Dn

C5Cr

C5Cn

C5Br

C5Bn

C5ADn

C5ADr


























M1

M2

M3

M4

M5

M6

M7

a

b

a

b

a

b

N4

N5

N6

N7

N8

N9

N10















NN2

NN3

NN4

NN5

CN1

CN2

CN3

CN4

ab

c

12

1

2

1

2

1

2

1

2

1

2

12

3

3

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)







C Neogene

Age

(M

a)








23

235

24

245

25

255

26

265

27

275

28

285

29

295

30

305

31

315

32

325

33

335

34

345

35

355

36

365

37

375

38

385

39

40

395

Pal

eoge

ne

Eoc

ene

Olig

ocen

e

Bar

toni

anP

riabo

nian

Rup

elia

nC

hatti

an

C18n

C17r

C17n

C16n

C16r

C15n

C15r

C13n

C13r

C12n

C12r

C11n

C11r

C10n

C10r

C9n

C9r

C8n

C8r

C7AnC7Ar

C7n

C7r

C6Cn

C6Cr


























E13

E14

E15

E16

O1

O2

O3

O4

O5

O6

O7

a

P14

P15

P16 P17

P18

P19

P20

P21

P22




























NP17

NP18

NP19-NP20

NP21

NP22

NP23

NP24

NP25

NN1

CP14

CP15

CP16

CP17

CP18

CP19

b

a

b

c

ab1

2

1

2

1

2

12

1

2

1

2

1

2

1

2

3

3

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)









D Paleogene

Age

(M

a)




















Triple combo

Caliper

HLDS(density)

EDTC(telemetry

gamma ray)

HRLA(resistivity)

3986 m

3854

3656

3299

2493

1950

1600

1372

635

407367

000

Centralizer

Knuckle joints

Cablehead

Pressurebulkhead

Centralizer

MSS(magnetic

susceptibility)

FMS-sonic


EDTC(telemetry

temperatureγ ray)

Centralizer

Cablehead

3544 m

3455

3257

2901

2673

1118

890

768

000



APS(porosity)

HNGS(spectral

gamma ray)

HNGS(spectral

gamma ray)

Centralizer

Seismic

VSISonde

Shuttle

1132 m

819

183

000

EDTC(telemetry

gamma ray)

Cablehead

Tool zero





(cm)

Vertical resolution

(cm)


(cm)















































































































































Introduction

Operations

Site locations






Lithostratigraphy



Core disturbances


Rationale


Units


Summary

Igneous rocks

Units

Volcanic rocks

Plutonic rocks

Textures

Alteration




Geochemistry


Pore fluid analysis






ICP-AES

Sample preparation


Physical properties



P-wave velocity




Sediment strength

Color reflectance

Paleomagnetism



Discrete samples






Sample coordinates

Core orientation

Magnetostratigraphy

Biostratigraphy


Foraminifers


Age model

Timescale

Depth scale





Wireline logging

Operations



Log data quality




References

Figures





















Tables




















Table of contents






















Volcaniccomponent





volcanic breccia














1984)






Ash tuff











conglomerate










2575

2575

7525

7525


TuffLapilli

Lapillistone

Ash-breccia

Tuff-breccia





Volcanic breccia


Lapilli2ndash64 mm

Ashlt2 mm


jim
Highlight
jim
Highlight
jim
Highlight






















Sorting

Rounding

















































A B

PumicePumice

1 mm 1 mm












Q

PA

90

60

20

5

90653510

Quartzolite

Granite

Monzogranite

Sye

nogr

anite

Quartz monozite

Syenite Monzonite

Granodiorite

Tonalite

Alka

li fe

ldsp

ar g

rani

te


A

Plagioclase


Orthopyroxene

Norite

NoriteW

ehrlite

Olivine

Clinopyroxenite

Oliv

ine

orth

opyr

oxen

ite

Har

zbur

gite

Gab

bro

Gab

bro



Lherzolite


Clinopyroxenite

Orthopyroxenite

Websterite

Gabbronorite

40

Clin

opyr

oxen

e

Anorthosite90

5

B




DioriteGabbro

Anorthosite



Olivinewebsterite




If phyric


































Sphericity

High

Moderate

Low

Elongate

Pipe

Rounded

Subrounded

Subangular

Angular

Very angular

Roundness




mio

cene

VI

1

2

3

4

5

6

7

0

100

200

300

400

500

600

700

800

900137750

137650

137550

137450

137350

137250

137150

137050

136950pumice

pumice

pumice

fiamme

pillow fragment

fiamme

fiamme

fiamme

pumicefiamme

pumice

pumice

pumice

XRF

TSBTS

MAD

HS

MAD

MAD

MAD

10-40

20-80

ReflectanceL a b


(cps)

40200

MS LoopMS Point

(SI)

20000

Age

Ship

boar

dsa

mpl

es

Sedi

men

tary

stru

ctur

es

Graphiclithology

CoreimageLi

thol

ogic

unit

Sect

ion

Core

leng

th (c

m)

Dept

h CS

F-A

(m)


Dist

urba

nce

type


Dom

inan

t vitr

ic

Grain size rankMax

Modal

1062

Gra

ding

Dom

inan

t

2nd

orde

r

3rd

orde

r

Component

Clos

ely

inte

rcal

ated






Finesand


Mud Sand Gravel

ClayClaystone

MudMudstone

100001

90002

80004

70008

60016

50031

40063

30125

20250

10500

01

-12

-24

-38

-416

-532

-664

-7128

-8256

-9512

Φmm

AshLapilli



SandSandstone

Evolved ashTuff


Bimodal ashTuff

Rhyoliteor

dacite



Mafic ashTuff

Monomicticbreccia




Evolved

Mafic


Fine ash Coarse ash

Very finesand

Mediumsand

Coarsesand

Very coarsesand

Boulder

Polymictic

Monomictic

Polymictic

Monomictic

Polymictic

Monomictic

Polymictic

Monomictic

Intermediateor

bimodal




Polymicticbreccia










Tuffaceous breccia




Disturbance type

Basal flow-in

Biscuit

Brecciated

Core extension

Fall-in

Fractured

Mid-core flow-in

Sediment flowage

Soupy

Void

Component

Lithic

Crystal

Vitric


Convolute bedded

Cross-bedded

Flame structure

Intraclast

Lenticular bedded


Stratified

Grading

Density graded

Normally graded

Reversely graded



















































0 20 40 60 80 10000

01

02

03

04

Y K

α (n

orm

aliz

ed to

Ag

Com

pton

)

Y standard (ppm)

y = 000387 times x


Oxi

de (

wt

)


Ele

men

t (p

pm)





n = 131

Y = 24 plusmn 3 ppm

03

04

05

90

95

100

105

410 417 424 51 58 515 522 5290

20

40

60

150

170

190








Ref

eren

ce


Standard

plusmn20 (rel)

000 005 010 015 020 025 030000

005

010

015

020

025

030

0 2 4 6 8 10 12 14 16 180

2

4

6

8

10

12

14

16

18

00 05 10 15 20 25 3000

05

10

15

20

25

30

Sr (ppm)

0 100 200 300 400 500 600 700 8000

100

200

300

400

500

600

700

800

CaO (wt)

0 2 4 6 8 10 12 140

2

4

6

8

10

12

14

Zn (ppm)

0 50 100 1500

50

100

150

Zr (ppm)

0 50 100 150 200 250 3000

50

100

150

200

250

300

K2O (wt)

0 1 2 3 4 500

05

10

15

20

25

30

35

40

45

50

Y (ppm)

0 10 20 30 40 50 60 700

10

20

30

40

50

60

70

pXRFICP-AES



















































q = k(dTdx)



T(t) = A1 + A2 ln(t) + A3 [ln(t)t] + (A4t)














ρwet = MwetVwet

ρdry = MsolidVwet


φ = VpwVwet

and

VR = VpwVsolid















































Working half

+x = north+y = east

Bottom

+z

+y

+xTop

Top

Upcore

Upcore

Bottom

+x+z

+y

Archive half

270deg

0deg

90deg

180deg

90deg270deg

N

E

S

W



Discrete sample

Up

Bottom Up arrow+z+y

+x

Japanese cube


A

B+z

+y

+x

+x +z

+y+z

+y

+x



















B 6252C3An2n T 6436

B 6733C3Bn T 7140

B 7212C3Br1n T 7251

B 7285C3Br2n T 7454

B 7489C4n1n T 7528

B 7642C4n2n T 7695

B 8108C4r1n T 8254

B 8300C4An T 8771

B 9105C4Ar1n T 9311

B 9426C4Ar2n T 9647

B 9721C5n1n T 9786

B 9937C5n2n T 9984

B 11056C5r1n T 11146

B 11188C5r2r-1n T 11263

B 11308C5r2n T 11592

B 11657C5An1n T 12049

B 12174C5An2n T 12272

B 12474C5Ar1n T 12735

B 12770C5Ar2n T 12829

B 12887C5AAn T 13032

B 13183

C5ABn T 13363B 13608

C5ACn T 13739B 14070

C5ADn T 14163B 14609

C5Bn1n T 14775B 14870

C5Bn2n T 15032B 15160

C5Cn1n T 15974B 16268

C4Cn2n T 16303B 16472

C5Cn3n T 16543B 16721

C5Dn T 17235B 17533

C5Dr1n T 17717B 17740

C5En T 18056B 18524

C6n T 18748B 19722

C6An1n T 20040B 20213

C6An2n T 20439B 20709

C6AAn T 21083B 21159

C6AAr1n T 21403B 21483

C6AAr2n T 21659B 21688

C6Bn1n T 21767B 21936

C6Bn1n T 21992B 22268

C6Cn1n T 22564B 22754

C6Cn2n T 22902B 23030

C6Cn3n T 23233B 23295

C7n1n T 23962B 24000

C7n2n T 24109B 24474

C7An T 24761B 24984

C81n T 25099B 25264

C82n T 25304B 25987

C9n T 26420B 27439

C10n1n T 27859B 28087

C10n2n T 28141B 28278

C11n1n T 29183




B 29477C11n2n T 29527

B 29970C12n T 30591

B 31034C13n T 33157

B 33705C15n T 34999

B 35294C16n1n T 35706

B 35892C16n2n T 36051

B 36700C17n1n T 36969

B 37753C17n2n T 37872

B 38093C17n3n T 38159

B 38333C18n1n T 38615

B 39627C18n2n T 39698

B 40145C19n T 41154

B 41390C20n T 42301

B 43432C21n T 45724

B 47349C22n T 48566

B 49344C23n1n T 50628

B 50835C23n2n T 50961

B 51833C24n1n T 52620

B 53074C24n2n T 53199

B 53274C24n3n T 53416

B 53983



















ZoneSubzone









































ZoneSubzone








ZoneSubzone





ZoneSubzone


(Ma)



























ZoneSubzone


(Ma)




























ZoneSubzone


(Ma)



T

CC n

CC n+1



B

CC n

CC n+1

1680

1685

2578

2583

+6490

6495

6500

6505



















Age

(M

a)



05

0

1

15

2

25

3

35

4

45

5

Qua

tern

ary

Plio

cene

Ple

isto

cene

Hol

Zan

clea

nP

iace

nzia

nG

elas

ian

Cal

abria

nIo

nian

Taran-tian

C3n

C2An

C2Ar

C2n

C2r

C1n

C1r



















PL1

PL2

PL3PL4

PL5

PL6

Pt1

a

b

N18 N19

N20 N21

N22



























NN12

NN13

NN14NN15

NN16

NN17

NN18

NN19

NN20

NN21

CN10

CN11

CN12

CN13

CN14

CN15

b

c

a

b

a

b

c

d

a

b

a

b

1

2

1

2

1

2

3

1

2

34

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)


Neo

gene











Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr

on




Age

(M

a)

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



55

6

65

7

75

8

85

9

95

10

105

11

115

12

125

13

135

14

Neo

gene

Mio

cene

Ser

rava

llian

Tort

onia

nM

essi

nian

C5ACn

C5ABnC5ABr

C5AAnC5AAr

C5An

C5Ar

C5n

C5r

C4An

C4Ar

C4r

C4n

C3BnC3Br

C3An

C3Ar




























M8

M9

M10

M11

M12

M13

M14

a

b

a

b

a

b

N10

N11

N12

N13

N14

N15

N16

N17





































NN5

NN6

NN7

NN8

NN9

NN10

NN11

NN12

CN4

CN5

CN6

CN7

CN8

CN9

a

b

a

b

c

d

a

1

1

2

1

2

1

2

1

2

1

2

1

2

1

2

3

3

1

2

2

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)












B Neogene








and




jim
Highlight
jim
Highlight
jim
Highlight
jim
Highlight



Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



14

145

15

155

16

165

17

175

18

185

19

195

20

205

21

215

22

225

23

Neo

gene

Mio

cene

Aqu

itani

anB

urdi

galia

nLa

nghi

an

C6Cn

C6Bn

C6Br

C6AAn

C6AAr

C6Ar

C6An

C6n

C6r

C5En

C5Er

C5Dr

C5Dn

C5Cr

C5Cn

C5Br

C5Bn

C5ADn

C5ADr


























M1

M2

M3

M4

M5

M6

M7

a

b

a

b

a

b

N4

N5

N6

N7

N8

N9

N10















NN2

NN3

NN4

NN5

CN1

CN2

CN3

CN4

ab

c

12

1

2

1

2

1

2

1

2

1

2

12

3

3

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)







C Neogene

Age

(M

a)








23

235

24

245

25

255

26

265

27

275

28

285

29

295

30

305

31

315

32

325

33

335

34

345

35

355

36

365

37

375

38

385

39

40

395

Pal

eoge

ne

Eoc

ene

Olig

ocen

e

Bar

toni

anP

riabo

nian

Rup

elia

nC

hatti

an

C18n

C17r

C17n

C16n

C16r

C15n

C15r

C13n

C13r

C12n

C12r

C11n

C11r

C10n

C10r

C9n

C9r

C8n

C8r

C7AnC7Ar

C7n

C7r

C6Cn

C6Cr


























E13

E14

E15

E16

O1

O2

O3

O4

O5

O6

O7

a

P14

P15

P16 P17

P18

P19

P20

P21

P22




























NP17

NP18

NP19-NP20

NP21

NP22

NP23

NP24

NP25

NN1

CP14

CP15

CP16

CP17

CP18

CP19

b

a

b

c

ab1

2

1

2

1

2

12

1

2

1

2

1

2

1

2

3

3

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)









D Paleogene

Age

(M

a)




















Triple combo

Caliper

HLDS(density)

EDTC(telemetry

gamma ray)

HRLA(resistivity)

3986 m

3854

3656

3299

2493

1950

1600

1372

635

407367

000

Centralizer

Knuckle joints

Cablehead

Pressurebulkhead

Centralizer

MSS(magnetic

susceptibility)

FMS-sonic


EDTC(telemetry

temperatureγ ray)

Centralizer

Cablehead

3544 m

3455

3257

2901

2673

1118

890

768

000



APS(porosity)

HNGS(spectral

gamma ray)

HNGS(spectral

gamma ray)

Centralizer

Seismic

VSISonde

Shuttle

1132 m

819

183

000

EDTC(telemetry

gamma ray)

Cablehead

Tool zero





(cm)

Vertical resolution

(cm)


(cm)















































































































































Introduction

Operations

Site locations






Lithostratigraphy



Core disturbances


Rationale


Units


Summary

Igneous rocks

Units

Volcanic rocks

Plutonic rocks

Textures

Alteration




Geochemistry


Pore fluid analysis






ICP-AES

Sample preparation


Physical properties



P-wave velocity




Sediment strength

Color reflectance

Paleomagnetism



Discrete samples






Sample coordinates

Core orientation

Magnetostratigraphy

Biostratigraphy


Foraminifers


Age model

Timescale

Depth scale





Wireline logging

Operations



Log data quality




References

Figures





















Tables




















Table of contents













1984)






Ash tuff











conglomerate










2575

2575

7525

7525


TuffLapilli

Lapillistone

Ash-breccia

Tuff-breccia





Volcanic breccia


Lapilli2ndash64 mm

Ashlt2 mm


jim
Highlight
jim
Highlight
jim
Highlight






















Sorting

Rounding

















































A B

PumicePumice

1 mm 1 mm












Q

PA

90

60

20

5

90653510

Quartzolite

Granite

Monzogranite

Sye

nogr

anite

Quartz monozite

Syenite Monzonite

Granodiorite

Tonalite

Alka

li fe

ldsp

ar g

rani

te


A

Plagioclase


Orthopyroxene

Norite

NoriteW

ehrlite

Olivine

Clinopyroxenite

Oliv

ine

orth

opyr

oxen

ite

Har

zbur

gite

Gab

bro

Gab

bro



Lherzolite


Clinopyroxenite

Orthopyroxenite

Websterite

Gabbronorite

40

Clin

opyr

oxen

e

Anorthosite90

5

B




DioriteGabbro

Anorthosite



Olivinewebsterite




If phyric


































Sphericity

High

Moderate

Low

Elongate

Pipe

Rounded

Subrounded

Subangular

Angular

Very angular

Roundness




mio

cene

VI

1

2

3

4

5

6

7

0

100

200

300

400

500

600

700

800

900137750

137650

137550

137450

137350

137250

137150

137050

136950pumice

pumice

pumice

fiamme

pillow fragment

fiamme

fiamme

fiamme

pumicefiamme

pumice

pumice

pumice

XRF

TSBTS

MAD

HS

MAD

MAD

MAD

10-40

20-80

ReflectanceL a b


(cps)

40200

MS LoopMS Point

(SI)

20000

Age

Ship

boar

dsa

mpl

es

Sedi

men

tary

stru

ctur

es

Graphiclithology

CoreimageLi

thol

ogic

unit

Sect

ion

Core

leng

th (c

m)

Dept

h CS

F-A

(m)


Dist

urba

nce

type


Dom

inan

t vitr

ic

Grain size rankMax

Modal

1062

Gra

ding

Dom

inan

t

2nd

orde

r

3rd

orde

r

Component

Clos

ely

inte

rcal

ated






Finesand


Mud Sand Gravel

ClayClaystone

MudMudstone

100001

90002

80004

70008

60016

50031

40063

30125

20250

10500

01

-12

-24

-38

-416

-532

-664

-7128

-8256

-9512

Φmm

AshLapilli



SandSandstone

Evolved ashTuff


Bimodal ashTuff

Rhyoliteor

dacite



Mafic ashTuff

Monomicticbreccia




Evolved

Mafic


Fine ash Coarse ash

Very finesand

Mediumsand

Coarsesand

Very coarsesand

Boulder

Polymictic

Monomictic

Polymictic

Monomictic

Polymictic

Monomictic

Polymictic

Monomictic

Intermediateor

bimodal




Polymicticbreccia










Tuffaceous breccia




Disturbance type

Basal flow-in

Biscuit

Brecciated

Core extension

Fall-in

Fractured

Mid-core flow-in

Sediment flowage

Soupy

Void

Component

Lithic

Crystal

Vitric


Convolute bedded

Cross-bedded

Flame structure

Intraclast

Lenticular bedded


Stratified

Grading

Density graded

Normally graded

Reversely graded



















































0 20 40 60 80 10000

01

02

03

04

Y K

α (n

orm

aliz

ed to

Ag

Com

pton

)

Y standard (ppm)

y = 000387 times x


Oxi

de (

wt

)


Ele

men

t (p

pm)





n = 131

Y = 24 plusmn 3 ppm

03

04

05

90

95

100

105

410 417 424 51 58 515 522 5290

20

40

60

150

170

190








Ref

eren

ce


Standard

plusmn20 (rel)

000 005 010 015 020 025 030000

005

010

015

020

025

030

0 2 4 6 8 10 12 14 16 180

2

4

6

8

10

12

14

16

18

00 05 10 15 20 25 3000

05

10

15

20

25

30

Sr (ppm)

0 100 200 300 400 500 600 700 8000

100

200

300

400

500

600

700

800

CaO (wt)

0 2 4 6 8 10 12 140

2

4

6

8

10

12

14

Zn (ppm)

0 50 100 1500

50

100

150

Zr (ppm)

0 50 100 150 200 250 3000

50

100

150

200

250

300

K2O (wt)

0 1 2 3 4 500

05

10

15

20

25

30

35

40

45

50

Y (ppm)

0 10 20 30 40 50 60 700

10

20

30

40

50

60

70

pXRFICP-AES



















































q = k(dTdx)



T(t) = A1 + A2 ln(t) + A3 [ln(t)t] + (A4t)














ρwet = MwetVwet

ρdry = MsolidVwet


φ = VpwVwet

and

VR = VpwVsolid















































Working half

+x = north+y = east

Bottom

+z

+y

+xTop

Top

Upcore

Upcore

Bottom

+x+z

+y

Archive half

270deg

0deg

90deg

180deg

90deg270deg

N

E

S

W



Discrete sample

Up

Bottom Up arrow+z+y

+x

Japanese cube


A

B+z

+y

+x

+x +z

+y+z

+y

+x



















B 6252C3An2n T 6436

B 6733C3Bn T 7140

B 7212C3Br1n T 7251

B 7285C3Br2n T 7454

B 7489C4n1n T 7528

B 7642C4n2n T 7695

B 8108C4r1n T 8254

B 8300C4An T 8771

B 9105C4Ar1n T 9311

B 9426C4Ar2n T 9647

B 9721C5n1n T 9786

B 9937C5n2n T 9984

B 11056C5r1n T 11146

B 11188C5r2r-1n T 11263

B 11308C5r2n T 11592

B 11657C5An1n T 12049

B 12174C5An2n T 12272

B 12474C5Ar1n T 12735

B 12770C5Ar2n T 12829

B 12887C5AAn T 13032

B 13183

C5ABn T 13363B 13608

C5ACn T 13739B 14070

C5ADn T 14163B 14609

C5Bn1n T 14775B 14870

C5Bn2n T 15032B 15160

C5Cn1n T 15974B 16268

C4Cn2n T 16303B 16472

C5Cn3n T 16543B 16721

C5Dn T 17235B 17533

C5Dr1n T 17717B 17740

C5En T 18056B 18524

C6n T 18748B 19722

C6An1n T 20040B 20213

C6An2n T 20439B 20709

C6AAn T 21083B 21159

C6AAr1n T 21403B 21483

C6AAr2n T 21659B 21688

C6Bn1n T 21767B 21936

C6Bn1n T 21992B 22268

C6Cn1n T 22564B 22754

C6Cn2n T 22902B 23030

C6Cn3n T 23233B 23295

C7n1n T 23962B 24000

C7n2n T 24109B 24474

C7An T 24761B 24984

C81n T 25099B 25264

C82n T 25304B 25987

C9n T 26420B 27439

C10n1n T 27859B 28087

C10n2n T 28141B 28278

C11n1n T 29183




B 29477C11n2n T 29527

B 29970C12n T 30591

B 31034C13n T 33157

B 33705C15n T 34999

B 35294C16n1n T 35706

B 35892C16n2n T 36051

B 36700C17n1n T 36969

B 37753C17n2n T 37872

B 38093C17n3n T 38159

B 38333C18n1n T 38615

B 39627C18n2n T 39698

B 40145C19n T 41154

B 41390C20n T 42301

B 43432C21n T 45724

B 47349C22n T 48566

B 49344C23n1n T 50628

B 50835C23n2n T 50961

B 51833C24n1n T 52620

B 53074C24n2n T 53199

B 53274C24n3n T 53416

B 53983



















ZoneSubzone









































ZoneSubzone








ZoneSubzone





ZoneSubzone


(Ma)



























ZoneSubzone


(Ma)




























ZoneSubzone


(Ma)



T

CC n

CC n+1



B

CC n

CC n+1

1680

1685

2578

2583

+6490

6495

6500

6505



















Age

(M

a)



05

0

1

15

2

25

3

35

4

45

5

Qua

tern

ary

Plio

cene

Ple

isto

cene

Hol

Zan

clea

nP

iace

nzia

nG

elas

ian

Cal

abria

nIo

nian

Taran-tian

C3n

C2An

C2Ar

C2n

C2r

C1n

C1r



















PL1

PL2

PL3PL4

PL5

PL6

Pt1

a

b

N18 N19

N20 N21

N22



























NN12

NN13

NN14NN15

NN16

NN17

NN18

NN19

NN20

NN21

CN10

CN11

CN12

CN13

CN14

CN15

b

c

a

b

a

b

c

d

a

b

a

b

1

2

1

2

1

2

3

1

2

34

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)


Neo

gene











Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr

on




Age

(M

a)

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



55

6

65

7

75

8

85

9

95

10

105

11

115

12

125

13

135

14

Neo

gene

Mio

cene

Ser

rava

llian

Tort

onia

nM

essi

nian

C5ACn

C5ABnC5ABr

C5AAnC5AAr

C5An

C5Ar

C5n

C5r

C4An

C4Ar

C4r

C4n

C3BnC3Br

C3An

C3Ar




























M8

M9

M10

M11

M12

M13

M14

a

b

a

b

a

b

N10

N11

N12

N13

N14

N15

N16

N17





































NN5

NN6

NN7

NN8

NN9

NN10

NN11

NN12

CN4

CN5

CN6

CN7

CN8

CN9

a

b

a

b

c

d

a

1

1

2

1

2

1

2

1

2

1

2

1

2

1

2

3

3

1

2

2

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)












B Neogene








and




jim
Highlight
jim
Highlight
jim
Highlight
jim
Highlight



Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



14

145

15

155

16

165

17

175

18

185

19

195

20

205

21

215

22

225

23

Neo

gene

Mio

cene

Aqu

itani

anB

urdi

galia

nLa

nghi

an

C6Cn

C6Bn

C6Br

C6AAn

C6AAr

C6Ar

C6An

C6n

C6r

C5En

C5Er

C5Dr

C5Dn

C5Cr

C5Cn

C5Br

C5Bn

C5ADn

C5ADr


























M1

M2

M3

M4

M5

M6

M7

a

b

a

b

a

b

N4

N5

N6

N7

N8

N9

N10















NN2

NN3

NN4

NN5

CN1

CN2

CN3

CN4

ab

c

12

1

2

1

2

1

2

1

2

1

2

12

3

3

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)







C Neogene

Age

(M

a)








23

235

24

245

25

255

26

265

27

275

28

285

29

295

30

305

31

315

32

325

33

335

34

345

35

355

36

365

37

375

38

385

39

40

395

Pal

eoge

ne

Eoc

ene

Olig

ocen

e

Bar

toni

anP

riabo

nian

Rup

elia

nC

hatti

an

C18n

C17r

C17n

C16n

C16r

C15n

C15r

C13n

C13r

C12n

C12r

C11n

C11r

C10n

C10r

C9n

C9r

C8n

C8r

C7AnC7Ar

C7n

C7r

C6Cn

C6Cr


























E13

E14

E15

E16

O1

O2

O3

O4

O5

O6

O7

a

P14

P15

P16 P17

P18

P19

P20

P21

P22




























NP17

NP18

NP19-NP20

NP21

NP22

NP23

NP24

NP25

NN1

CP14

CP15

CP16

CP17

CP18

CP19

b

a

b

c

ab1

2

1

2

1

2

12

1

2

1

2

1

2

1

2

3

3

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)









D Paleogene

Age

(M

a)




















Triple combo

Caliper

HLDS(density)

EDTC(telemetry

gamma ray)

HRLA(resistivity)

3986 m

3854

3656

3299

2493

1950

1600

1372

635

407367

000

Centralizer

Knuckle joints

Cablehead

Pressurebulkhead

Centralizer

MSS(magnetic

susceptibility)

FMS-sonic


EDTC(telemetry

temperatureγ ray)

Centralizer

Cablehead

3544 m

3455

3257

2901

2673

1118

890

768

000



APS(porosity)

HNGS(spectral

gamma ray)

HNGS(spectral

gamma ray)

Centralizer

Seismic

VSISonde

Shuttle

1132 m

819

183

000

EDTC(telemetry

gamma ray)

Cablehead

Tool zero





(cm)

Vertical resolution

(cm)


(cm)















































































































































Introduction

Operations

Site locations






Lithostratigraphy



Core disturbances


Rationale


Units


Summary

Igneous rocks

Units

Volcanic rocks

Plutonic rocks

Textures

Alteration




Geochemistry


Pore fluid analysis






ICP-AES

Sample preparation


Physical properties



P-wave velocity




Sediment strength

Color reflectance

Paleomagnetism



Discrete samples






Sample coordinates

Core orientation

Magnetostratigraphy

Biostratigraphy


Foraminifers


Age model

Timescale

Depth scale





Wireline logging

Operations



Log data quality




References

Figures





















Tables




















Table of contents






















Sorting

Rounding

















































A B

PumicePumice

1 mm 1 mm












Q

PA

90

60

20

5

90653510

Quartzolite

Granite

Monzogranite

Sye

nogr

anite

Quartz monozite

Syenite Monzonite

Granodiorite

Tonalite

Alka

li fe

ldsp

ar g

rani

te


A

Plagioclase


Orthopyroxene

Norite

NoriteW

ehrlite

Olivine

Clinopyroxenite

Oliv

ine

orth

opyr

oxen

ite

Har

zbur

gite

Gab

bro

Gab

bro



Lherzolite


Clinopyroxenite

Orthopyroxenite

Websterite

Gabbronorite

40

Clin

opyr

oxen

e

Anorthosite90

5

B




DioriteGabbro

Anorthosite



Olivinewebsterite




If phyric


































Sphericity

High

Moderate

Low

Elongate

Pipe

Rounded

Subrounded

Subangular

Angular

Very angular

Roundness




mio

cene

VI

1

2

3

4

5

6

7

0

100

200

300

400

500

600

700

800

900137750

137650

137550

137450

137350

137250

137150

137050

136950pumice

pumice

pumice

fiamme

pillow fragment

fiamme

fiamme

fiamme

pumicefiamme

pumice

pumice

pumice

XRF

TSBTS

MAD

HS

MAD

MAD

MAD

10-40

20-80

ReflectanceL a b


(cps)

40200

MS LoopMS Point

(SI)

20000

Age

Ship

boar

dsa

mpl

es

Sedi

men

tary

stru

ctur

es

Graphiclithology

CoreimageLi

thol

ogic

unit

Sect

ion

Core

leng

th (c

m)

Dept

h CS

F-A

(m)


Dist

urba

nce

type


Dom

inan

t vitr

ic

Grain size rankMax

Modal

1062

Gra

ding

Dom

inan

t

2nd

orde

r

3rd

orde

r

Component

Clos

ely

inte

rcal

ated






Finesand


Mud Sand Gravel

ClayClaystone

MudMudstone

100001

90002

80004

70008

60016

50031

40063

30125

20250

10500

01

-12

-24

-38

-416

-532

-664

-7128

-8256

-9512

Φmm

AshLapilli



SandSandstone

Evolved ashTuff


Bimodal ashTuff

Rhyoliteor

dacite



Mafic ashTuff

Monomicticbreccia




Evolved

Mafic


Fine ash Coarse ash

Very finesand

Mediumsand

Coarsesand

Very coarsesand

Boulder

Polymictic

Monomictic

Polymictic

Monomictic

Polymictic

Monomictic

Polymictic

Monomictic

Intermediateor

bimodal




Polymicticbreccia










Tuffaceous breccia




Disturbance type

Basal flow-in

Biscuit

Brecciated

Core extension

Fall-in

Fractured

Mid-core flow-in

Sediment flowage

Soupy

Void

Component

Lithic

Crystal

Vitric


Convolute bedded

Cross-bedded

Flame structure

Intraclast

Lenticular bedded


Stratified

Grading

Density graded

Normally graded

Reversely graded



















































0 20 40 60 80 10000

01

02

03

04

Y K

α (n

orm

aliz

ed to

Ag

Com

pton

)

Y standard (ppm)

y = 000387 times x


Oxi

de (

wt

)


Ele

men

t (p

pm)





n = 131

Y = 24 plusmn 3 ppm

03

04

05

90

95

100

105

410 417 424 51 58 515 522 5290

20

40

60

150

170

190








Ref

eren

ce


Standard

plusmn20 (rel)

000 005 010 015 020 025 030000

005

010

015

020

025

030

0 2 4 6 8 10 12 14 16 180

2

4

6

8

10

12

14

16

18

00 05 10 15 20 25 3000

05

10

15

20

25

30

Sr (ppm)

0 100 200 300 400 500 600 700 8000

100

200

300

400

500

600

700

800

CaO (wt)

0 2 4 6 8 10 12 140

2

4

6

8

10

12

14

Zn (ppm)

0 50 100 1500

50

100

150

Zr (ppm)

0 50 100 150 200 250 3000

50

100

150

200

250

300

K2O (wt)

0 1 2 3 4 500

05

10

15

20

25

30

35

40

45

50

Y (ppm)

0 10 20 30 40 50 60 700

10

20

30

40

50

60

70

pXRFICP-AES



















































q = k(dTdx)



T(t) = A1 + A2 ln(t) + A3 [ln(t)t] + (A4t)














ρwet = MwetVwet

ρdry = MsolidVwet


φ = VpwVwet

and

VR = VpwVsolid















































Working half

+x = north+y = east

Bottom

+z

+y

+xTop

Top

Upcore

Upcore

Bottom

+x+z

+y

Archive half

270deg

0deg

90deg

180deg

90deg270deg

N

E

S

W



Discrete sample

Up

Bottom Up arrow+z+y

+x

Japanese cube


A

B+z

+y

+x

+x +z

+y+z

+y

+x



















B 6252C3An2n T 6436

B 6733C3Bn T 7140

B 7212C3Br1n T 7251

B 7285C3Br2n T 7454

B 7489C4n1n T 7528

B 7642C4n2n T 7695

B 8108C4r1n T 8254

B 8300C4An T 8771

B 9105C4Ar1n T 9311

B 9426C4Ar2n T 9647

B 9721C5n1n T 9786

B 9937C5n2n T 9984

B 11056C5r1n T 11146

B 11188C5r2r-1n T 11263

B 11308C5r2n T 11592

B 11657C5An1n T 12049

B 12174C5An2n T 12272

B 12474C5Ar1n T 12735

B 12770C5Ar2n T 12829

B 12887C5AAn T 13032

B 13183

C5ABn T 13363B 13608

C5ACn T 13739B 14070

C5ADn T 14163B 14609

C5Bn1n T 14775B 14870

C5Bn2n T 15032B 15160

C5Cn1n T 15974B 16268

C4Cn2n T 16303B 16472

C5Cn3n T 16543B 16721

C5Dn T 17235B 17533

C5Dr1n T 17717B 17740

C5En T 18056B 18524

C6n T 18748B 19722

C6An1n T 20040B 20213

C6An2n T 20439B 20709

C6AAn T 21083B 21159

C6AAr1n T 21403B 21483

C6AAr2n T 21659B 21688

C6Bn1n T 21767B 21936

C6Bn1n T 21992B 22268

C6Cn1n T 22564B 22754

C6Cn2n T 22902B 23030

C6Cn3n T 23233B 23295

C7n1n T 23962B 24000

C7n2n T 24109B 24474

C7An T 24761B 24984

C81n T 25099B 25264

C82n T 25304B 25987

C9n T 26420B 27439

C10n1n T 27859B 28087

C10n2n T 28141B 28278

C11n1n T 29183




B 29477C11n2n T 29527

B 29970C12n T 30591

B 31034C13n T 33157

B 33705C15n T 34999

B 35294C16n1n T 35706

B 35892C16n2n T 36051

B 36700C17n1n T 36969

B 37753C17n2n T 37872

B 38093C17n3n T 38159

B 38333C18n1n T 38615

B 39627C18n2n T 39698

B 40145C19n T 41154

B 41390C20n T 42301

B 43432C21n T 45724

B 47349C22n T 48566

B 49344C23n1n T 50628

B 50835C23n2n T 50961

B 51833C24n1n T 52620

B 53074C24n2n T 53199

B 53274C24n3n T 53416

B 53983



















ZoneSubzone









































ZoneSubzone








ZoneSubzone





ZoneSubzone


(Ma)



























ZoneSubzone


(Ma)




























ZoneSubzone


(Ma)



T

CC n

CC n+1



B

CC n

CC n+1

1680

1685

2578

2583

+6490

6495

6500

6505



















Age

(M

a)



05

0

1

15

2

25

3

35

4

45

5

Qua

tern

ary

Plio

cene

Ple

isto

cene

Hol

Zan

clea

nP

iace

nzia

nG

elas

ian

Cal

abria

nIo

nian

Taran-tian

C3n

C2An

C2Ar

C2n

C2r

C1n

C1r



















PL1

PL2

PL3PL4

PL5

PL6

Pt1

a

b

N18 N19

N20 N21

N22



























NN12

NN13

NN14NN15

NN16

NN17

NN18

NN19

NN20

NN21

CN10

CN11

CN12

CN13

CN14

CN15

b

c

a

b

a

b

c

d

a

b

a

b

1

2

1

2

1

2

3

1

2

34

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)


Neo

gene











Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr

on




Age

(M

a)

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



55

6

65

7

75

8

85

9

95

10

105

11

115

12

125

13

135

14

Neo

gene

Mio

cene

Ser

rava

llian

Tort

onia

nM

essi

nian

C5ACn

C5ABnC5ABr

C5AAnC5AAr

C5An

C5Ar

C5n

C5r

C4An

C4Ar

C4r

C4n

C3BnC3Br

C3An

C3Ar




























M8

M9

M10

M11

M12

M13

M14

a

b

a

b

a

b

N10

N11

N12

N13

N14

N15

N16

N17





































NN5

NN6

NN7

NN8

NN9

NN10

NN11

NN12

CN4

CN5

CN6

CN7

CN8

CN9

a

b

a

b

c

d

a

1

1

2

1

2

1

2

1

2

1

2

1

2

1

2

3

3

1

2

2

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)












B Neogene








and




jim
Highlight
jim
Highlight
jim
Highlight
jim
Highlight



Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



14

145

15

155

16

165

17

175

18

185

19

195

20

205

21

215

22

225

23

Neo

gene

Mio

cene

Aqu

itani

anB

urdi

galia

nLa

nghi

an

C6Cn

C6Bn

C6Br

C6AAn

C6AAr

C6Ar

C6An

C6n

C6r

C5En

C5Er

C5Dr

C5Dn

C5Cr

C5Cn

C5Br

C5Bn

C5ADn

C5ADr


























M1

M2

M3

M4

M5

M6

M7

a

b

a

b

a

b

N4

N5

N6

N7

N8

N9

N10















NN2

NN3

NN4

NN5

CN1

CN2

CN3

CN4

ab

c

12

1

2

1

2

1

2

1

2

1

2

12

3

3

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)







C Neogene

Age

(M

a)








23

235

24

245

25

255

26

265

27

275

28

285

29

295

30

305

31

315

32

325

33

335

34

345

35

355

36

365

37

375

38

385

39

40

395

Pal

eoge

ne

Eoc

ene

Olig

ocen

e

Bar

toni

anP

riabo

nian

Rup

elia

nC

hatti

an

C18n

C17r

C17n

C16n

C16r

C15n

C15r

C13n

C13r

C12n

C12r

C11n

C11r

C10n

C10r

C9n

C9r

C8n

C8r

C7AnC7Ar

C7n

C7r

C6Cn

C6Cr


























E13

E14

E15

E16

O1

O2

O3

O4

O5

O6

O7

a

P14

P15

P16 P17

P18

P19

P20

P21

P22




























NP17

NP18

NP19-NP20

NP21

NP22

NP23

NP24

NP25

NN1

CP14

CP15

CP16

CP17

CP18

CP19

b

a

b

c

ab1

2

1

2

1

2

12

1

2

1

2

1

2

1

2

3

3

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)









D Paleogene

Age

(M

a)




















Triple combo

Caliper

HLDS(density)

EDTC(telemetry

gamma ray)

HRLA(resistivity)

3986 m

3854

3656

3299

2493

1950

1600

1372

635

407367

000

Centralizer

Knuckle joints

Cablehead

Pressurebulkhead

Centralizer

MSS(magnetic

susceptibility)

FMS-sonic


EDTC(telemetry

temperatureγ ray)

Centralizer

Cablehead

3544 m

3455

3257

2901

2673

1118

890

768

000



APS(porosity)

HNGS(spectral

gamma ray)

HNGS(spectral

gamma ray)

Centralizer

Seismic

VSISonde

Shuttle

1132 m

819

183

000

EDTC(telemetry

gamma ray)

Cablehead

Tool zero





(cm)

Vertical resolution

(cm)


(cm)















































































































































Introduction

Operations

Site locations






Lithostratigraphy



Core disturbances


Rationale


Units


Summary

Igneous rocks

Units

Volcanic rocks

Plutonic rocks

Textures

Alteration




Geochemistry


Pore fluid analysis






ICP-AES

Sample preparation


Physical properties



P-wave velocity




Sediment strength

Color reflectance

Paleomagnetism



Discrete samples






Sample coordinates

Core orientation

Magnetostratigraphy

Biostratigraphy


Foraminifers


Age model

Timescale

Depth scale





Wireline logging

Operations



Log data quality




References

Figures





















Tables




















Table of contents












































A B

PumicePumice

1 mm 1 mm












Q

PA

90

60

20

5

90653510

Quartzolite

Granite

Monzogranite

Sye

nogr

anite

Quartz monozite

Syenite Monzonite

Granodiorite

Tonalite

Alka

li fe

ldsp

ar g

rani

te


A

Plagioclase


Orthopyroxene

Norite

NoriteW

ehrlite

Olivine

Clinopyroxenite

Oliv

ine

orth

opyr

oxen

ite

Har

zbur

gite

Gab

bro

Gab

bro



Lherzolite


Clinopyroxenite

Orthopyroxenite

Websterite

Gabbronorite

40

Clin

opyr

oxen

e

Anorthosite90

5

B




DioriteGabbro

Anorthosite



Olivinewebsterite




If phyric


































Sphericity

High

Moderate

Low

Elongate

Pipe

Rounded

Subrounded

Subangular

Angular

Very angular

Roundness




mio

cene

VI

1

2

3

4

5

6

7

0

100

200

300

400

500

600

700

800

900137750

137650

137550

137450

137350

137250

137150

137050

136950pumice

pumice

pumice

fiamme

pillow fragment

fiamme

fiamme

fiamme

pumicefiamme

pumice

pumice

pumice

XRF

TSBTS

MAD

HS

MAD

MAD

MAD

10-40

20-80

ReflectanceL a b


(cps)

40200

MS LoopMS Point

(SI)

20000

Age

Ship

boar

dsa

mpl

es

Sedi

men

tary

stru

ctur

es

Graphiclithology

CoreimageLi

thol

ogic

unit

Sect

ion

Core

leng

th (c

m)

Dept

h CS

F-A

(m)


Dist

urba

nce

type


Dom

inan

t vitr

ic

Grain size rankMax

Modal

1062

Gra

ding

Dom

inan

t

2nd

orde

r

3rd

orde

r

Component

Clos

ely

inte

rcal

ated






Finesand


Mud Sand Gravel

ClayClaystone

MudMudstone

100001

90002

80004

70008

60016

50031

40063

30125

20250

10500

01

-12

-24

-38

-416

-532

-664

-7128

-8256

-9512

Φmm

AshLapilli



SandSandstone

Evolved ashTuff


Bimodal ashTuff

Rhyoliteor

dacite



Mafic ashTuff

Monomicticbreccia




Evolved

Mafic


Fine ash Coarse ash

Very finesand

Mediumsand

Coarsesand

Very coarsesand

Boulder

Polymictic

Monomictic

Polymictic

Monomictic

Polymictic

Monomictic

Polymictic

Monomictic

Intermediateor

bimodal




Polymicticbreccia










Tuffaceous breccia




Disturbance type

Basal flow-in

Biscuit

Brecciated

Core extension

Fall-in

Fractured

Mid-core flow-in

Sediment flowage

Soupy

Void

Component

Lithic

Crystal

Vitric


Convolute bedded

Cross-bedded

Flame structure

Intraclast

Lenticular bedded


Stratified

Grading

Density graded

Normally graded

Reversely graded



















































0 20 40 60 80 10000

01

02

03

04

Y K

α (n

orm

aliz

ed to

Ag

Com

pton

)

Y standard (ppm)

y = 000387 times x


Oxi

de (

wt

)


Ele

men

t (p

pm)





n = 131

Y = 24 plusmn 3 ppm

03

04

05

90

95

100

105

410 417 424 51 58 515 522 5290

20

40

60

150

170

190








Ref

eren

ce


Standard

plusmn20 (rel)

000 005 010 015 020 025 030000

005

010

015

020

025

030

0 2 4 6 8 10 12 14 16 180

2

4

6

8

10

12

14

16

18

00 05 10 15 20 25 3000

05

10

15

20

25

30

Sr (ppm)

0 100 200 300 400 500 600 700 8000

100

200

300

400

500

600

700

800

CaO (wt)

0 2 4 6 8 10 12 140

2

4

6

8

10

12

14

Zn (ppm)

0 50 100 1500

50

100

150

Zr (ppm)

0 50 100 150 200 250 3000

50

100

150

200

250

300

K2O (wt)

0 1 2 3 4 500

05

10

15

20

25

30

35

40

45

50

Y (ppm)

0 10 20 30 40 50 60 700

10

20

30

40

50

60

70

pXRFICP-AES



















































q = k(dTdx)



T(t) = A1 + A2 ln(t) + A3 [ln(t)t] + (A4t)














ρwet = MwetVwet

ρdry = MsolidVwet


φ = VpwVwet

and

VR = VpwVsolid















































Working half

+x = north+y = east

Bottom

+z

+y

+xTop

Top

Upcore

Upcore

Bottom

+x+z

+y

Archive half

270deg

0deg

90deg

180deg

90deg270deg

N

E

S

W



Discrete sample

Up

Bottom Up arrow+z+y

+x

Japanese cube


A

B+z

+y

+x

+x +z

+y+z

+y

+x



















B 6252C3An2n T 6436

B 6733C3Bn T 7140

B 7212C3Br1n T 7251

B 7285C3Br2n T 7454

B 7489C4n1n T 7528

B 7642C4n2n T 7695

B 8108C4r1n T 8254

B 8300C4An T 8771

B 9105C4Ar1n T 9311

B 9426C4Ar2n T 9647

B 9721C5n1n T 9786

B 9937C5n2n T 9984

B 11056C5r1n T 11146

B 11188C5r2r-1n T 11263

B 11308C5r2n T 11592

B 11657C5An1n T 12049

B 12174C5An2n T 12272

B 12474C5Ar1n T 12735

B 12770C5Ar2n T 12829

B 12887C5AAn T 13032

B 13183

C5ABn T 13363B 13608

C5ACn T 13739B 14070

C5ADn T 14163B 14609

C5Bn1n T 14775B 14870

C5Bn2n T 15032B 15160

C5Cn1n T 15974B 16268

C4Cn2n T 16303B 16472

C5Cn3n T 16543B 16721

C5Dn T 17235B 17533

C5Dr1n T 17717B 17740

C5En T 18056B 18524

C6n T 18748B 19722

C6An1n T 20040B 20213

C6An2n T 20439B 20709

C6AAn T 21083B 21159

C6AAr1n T 21403B 21483

C6AAr2n T 21659B 21688

C6Bn1n T 21767B 21936

C6Bn1n T 21992B 22268

C6Cn1n T 22564B 22754

C6Cn2n T 22902B 23030

C6Cn3n T 23233B 23295

C7n1n T 23962B 24000

C7n2n T 24109B 24474

C7An T 24761B 24984

C81n T 25099B 25264

C82n T 25304B 25987

C9n T 26420B 27439

C10n1n T 27859B 28087

C10n2n T 28141B 28278

C11n1n T 29183




B 29477C11n2n T 29527

B 29970C12n T 30591

B 31034C13n T 33157

B 33705C15n T 34999

B 35294C16n1n T 35706

B 35892C16n2n T 36051

B 36700C17n1n T 36969

B 37753C17n2n T 37872

B 38093C17n3n T 38159

B 38333C18n1n T 38615

B 39627C18n2n T 39698

B 40145C19n T 41154

B 41390C20n T 42301

B 43432C21n T 45724

B 47349C22n T 48566

B 49344C23n1n T 50628

B 50835C23n2n T 50961

B 51833C24n1n T 52620

B 53074C24n2n T 53199

B 53274C24n3n T 53416

B 53983



















ZoneSubzone









































ZoneSubzone








ZoneSubzone





ZoneSubzone


(Ma)



























ZoneSubzone


(Ma)




























ZoneSubzone


(Ma)



T

CC n

CC n+1



B

CC n

CC n+1

1680

1685

2578

2583

+6490

6495

6500

6505



















Age

(M

a)



05

0

1

15

2

25

3

35

4

45

5

Qua

tern

ary

Plio

cene

Ple

isto

cene

Hol

Zan

clea

nP

iace

nzia

nG

elas

ian

Cal

abria

nIo

nian

Taran-tian

C3n

C2An

C2Ar

C2n

C2r

C1n

C1r



















PL1

PL2

PL3PL4

PL5

PL6

Pt1

a

b

N18 N19

N20 N21

N22



























NN12

NN13

NN14NN15

NN16

NN17

NN18

NN19

NN20

NN21

CN10

CN11

CN12

CN13

CN14

CN15

b

c

a

b

a

b

c

d

a

b

a

b

1

2

1

2

1

2

3

1

2

34

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)


Neo

gene











Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr

on




Age

(M

a)

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



55

6

65

7

75

8

85

9

95

10

105

11

115

12

125

13

135

14

Neo

gene

Mio

cene

Ser

rava

llian

Tort

onia

nM

essi

nian

C5ACn

C5ABnC5ABr

C5AAnC5AAr

C5An

C5Ar

C5n

C5r

C4An

C4Ar

C4r

C4n

C3BnC3Br

C3An

C3Ar




























M8

M9

M10

M11

M12

M13

M14

a

b

a

b

a

b

N10

N11

N12

N13

N14

N15

N16

N17





































NN5

NN6

NN7

NN8

NN9

NN10

NN11

NN12

CN4

CN5

CN6

CN7

CN8

CN9

a

b

a

b

c

d

a

1

1

2

1

2

1

2

1

2

1

2

1

2

1

2

3

3

1

2

2

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)












B Neogene








and




jim
Highlight
jim
Highlight
jim
Highlight
jim
Highlight



Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



14

145

15

155

16

165

17

175

18

185

19

195

20

205

21

215

22

225

23

Neo

gene

Mio

cene

Aqu

itani

anB

urdi

galia

nLa

nghi

an

C6Cn

C6Bn

C6Br

C6AAn

C6AAr

C6Ar

C6An

C6n

C6r

C5En

C5Er

C5Dr

C5Dn

C5Cr

C5Cn

C5Br

C5Bn

C5ADn

C5ADr


























M1

M2

M3

M4

M5

M6

M7

a

b

a

b

a

b

N4

N5

N6

N7

N8

N9

N10















NN2

NN3

NN4

NN5

CN1

CN2

CN3

CN4

ab

c

12

1

2

1

2

1

2

1

2

1

2

12

3

3

Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)







C Neogene

Age

(M

a)








23

235

24

245

25

255

26

265

27

275

28

285

29

295

30

305

31

315

32

325

33

335

34

345

35

355

36

365

37

375

38

385

39

40

395

Pal

eoge

ne

Eoc

ene

Olig

ocen

e

Bar

toni

anP

riabo

nian

Rup

elia

nC

hatti

an

C18n

C17r

C17n

C16n

C16r

C15n

C15r

C13n

C13r

C12n

C12r

C11n

C11r

C10n

C10r

C9n

C9r

C8n

C8r

C7AnC7Ar

C7n

C7r

C6Cn

C6Cr


























E13

E14

E15

E16

O1

O2

O3

O4

O5

O6

O7

a

P14

P15

P16 P17

P18

P19

P20

P21

P22




























NP17

NP18

NP19-NP20

NP21

NP22

NP23

NP24

NP25

NN1

CP14

CP15

CP16

CP17

CP18

CP19

b

a

b

c

ab1

2

1

2

1

2

12

1

2

1

2

1

2

1

2

3

3

Per

iod

Epo

ch

Age

Sta

ge

Pol

arity

Chr



Berggrenet al

(1995)

Martini(1971)

Wadeet al

(2011)









D Paleogene

Age

(M

a)




















Triple combo

Caliper

HLDS(density)

EDTC(telemetry

gamma ray)

HRLA(resistivity)

3986 m

3854

3656

3299

2493

1950

1600

1372

635

407367

000

Centralizer

Knuckle joints

Cablehead

Pressurebulkhead

Centralizer

MSS(magnetic

susceptibility)

FMS-sonic


EDTC(telemetry

temperatureγ ray)

Centralizer

Cablehead

3544 m

3455

3257

2901

2673

1118

890

768

000



APS(porosity)

HNGS(spectral

gamma ray)

HNGS(spectral

gamma ray)

Centralizer

Seismic

VSISonde

Shuttle

1132 m

819

183

000

EDTC(telemetry

gamma ray)

Cablehead

Tool zero





(cm)

Vertical resolution

(cm)


(cm)















































































































































Introduction

Operations

Site locations






Lithostratigraphy



Core disturbances


Rationale


Units


Summary

Igneous rocks

Units

Volcanic rocks

Plutonic rocks

Textures

Alteration




Geochemistry


Pore fluid analysis






ICP-AES

Sample preparation


Physical properties



P-wave velocity




Sediment strength

Color reflectance

Paleomagnetism



Discrete samples






Sample coordinates

Core orientation

Magnetostratigraphy

Biostratigraphy


Foraminifers


Age model

Timescale

Depth scale





Wireline logging

Operations



Log data quality




References

Figures





















Tables




















Table of contents

Expedition 350 methods - University of Tasmania

Documents

Transcript of Expedition 350 methods - University of Tasmania