13. SITE 96

The Shipboard Scientific Party1

SITE DATAOccupied: March 30-31, 1970.

Position: 23°44.56'N;85°45.80'W.

Water Depth: 3439 meters.

Total Depth: 332 meters.

Holes Drilled: One.

Cores Taken: Five.

BACKGROUND AND OBJECTIVES

Three topographic highs in the western end of theStraits of Florida and southeastern Gulf of Mexico havebeen surveyed by Pyle et al. (1969) and Bryant et al.(1969). Each of these three structures, called JordanKnoll, Pinar del Rio Knoll, and Catoche Knoll, have apositive magnetic anomaly associated with it. All otherfeatures of similar structural outline in the Gulf basin havebeen associated with salt tectonics; however, the knolls ofthe southeastern Gulf of Mexico, due to the presence ofthe positive magnetic anomalies, are suspected of beingmainly results of igneous intrusions.

A positive total intensity magnetic anomaly of approxi-mately 200 gammas is associated with Jordan Knoll, whilepositive magnetic anomalies of from 100 to 200 gammashave been associated with the other two knolls. (Pyle etal., 1969).

A knoll located at the mouth of Catoche Tongue, withsmall surface relief (10 fathoms) was reported by theU.S.S. Kane during a geophysical cruise in 1969. Theknoll, selected from Site 96, lies within the "belt of volcan-ic-type anomalies" as reported by Gough (1967).

It had been suggested by Pyle et al. (1969) and Bryantet al. (1969) that Jordan Knoll, Pinar del Rio Knoll, andCatoche Knoll are igneous instrusions, because of the fol-lowing:

1) Pinar del Rio and Jordan knolls lie along a line ofextension of an axial valley anomaly and parallel the out-crop of ultramafic rocks of Cuba.

2) A positive magnetic anomaly is associated with suchfeatures.

3) Catoche Knoll is located within Gough's belt ofvolcanic-type anomalies.

J. Lamar Worzel, Marine Biomedical Institute, University ofTexas, Galveston; William Bryant, Texas A&M University (co-chiefscientists); Arthur O. Beall, Jr., Continental Oil Company (leadsedimentologist); Kendell Dickinson, United States GeologicalSurvey; Robert Laury, Southern Methodist University; Lee Ander-son Smith, ESSO Production Research (lead paleontologist); BlakeMcNeely, Shell Oil Company; Helen P. Foreman, Oberlin College;Roy Capo, Lamont-Doherty Geological Observatory.

4) No salt structures are known to occur within theGulf Basin east of a line from Campeche Canyon to DeSoto Canyon. A definite origin for the diapiric structuresin the southeastern Gulf cannot be forthcoming until suchstructures are drilled and sampled to their core. The ques-tion of their origin is obviously important in considera-tions of salt distribution and the history of the Gulf ofMexico.

It was decided that drilling one of these diapiric struc-tures would best be accomplished if the structure wasoutside the main flow of the Gulf Stream, had sufficientsediment cover to bury the bottom assembly before en-countering hard material, and had been surveyed with theaid of satellite navigation. Thus, the knoll in the CatocheTongue area, surveyed by the U.S.S. Kane, was chosen asSite 96.

The main objective at Site 96 was to drill to the coreof the knoll, a depth of approximately 350 meters, andobtain samples of material which would aid in determin-ing the origin of the structure. A coring inventory is givenin Table 1.

NATURE OF SEDIMENTS

General Description

Based on somewhat widely spaced sampling, Site 96appears to be in a rather thick sequence of Upper Pleisto-cene, terrigenous laminite clays and associated quartzoseturbidites overlying a thick sequence of lower Tertiarynannofossil ooze and chalk, locally chert bearing. In con-junction with an interpretation of the profiler record (seeObjectives), the structure on which Site 96 was drilled isinterpreted as a basement knoll (possibly Early Cretaceousin age?) on which was deposited considerable lowerTertiary (and possibly Upper Cretaceous?) pelagic ooze.

Through pelagic nondeposition, erosion, or subsidence,the knoll was more or less buried in Late Pleistocene timeby "typical" abyssal plain clay, mud, and associated tur-bidity current deposits. Normal consolidation around theflanks of the structure has apparently preserved minorrelief on the sea floor. Alternatively, the relief of the seafloor suggests the possibility that Core 1 could have beendeposited up to 16 meters or more above the surroundingabyssal plain. It could then be argued that turbidity cur-rents carry very fine sand in suspensions at least 16 metersthick.

Core 1 recovered olive gray to dark olive gray, massiveto occasionally laminated, terrigenous clay, with occa-sional graded muddy silt laminae and rare quartzose,sandy, coarse silt, graded beds. This sequence is inter-preted as a laminite-turbidite facies assemblage. The un-derlying sediments of Cores 2, 3, 4, and 5 are very lightgreenish white to very light yellow white (at the base),

297

SITE 96

TABLE 1Core Inventory - Site 96

Core

1

2

3

4

5

Total

% Cored

% Recovered

No.Sections

6

6

6

1

19

Date

3/30

3/30

3/31

3/31

3/31

Time

1900

2215

0130

0430

Coreda

Interval(m)

3540-3549

3638-3647

3740-3749

3760-3768

3768-3771

Cored(m)

9.0

9.0

9.0

8.0

3.0

38.0

11.4%

Recovered(m)

7.7

9.3

9.3

0.6b

1.0

27.3

71.8%

SubbottomPenetration

(m)

Top

101.0

199.0

301.0

321.0

329.0

Bottom

110.0

208.0

310.0

329.0

332.0

332.9

Lithology

Clay

ForamNanno ooze

ForamNanno chalk

ForamNanno chalk

ForamNanno chalk

Age

EarlyPleistocene

EarlyOligocene

EarlyEocene

LatePaleocene

LatePaleocene

Drill Pipe measurement from derrick floor.

Core catcher recovery only.

strongly burrowed, foraminiferal, nannofossil ooze andsoft chalk. Cores 2 and 4 contain greenish gray, calcareouschert. Core 2 also contains a few zones of burrow-mixedvolcanic ash. The first appearance of soft chalk was notedin Core 3, although Core 2 is quite mechanically disturbedand could be of an intermediate state of consolidation(tending toward chalk).

Sedimentological Interpretation

The presence of lower Tertiary pelagic oozes at Site 96suggests considerable relief on the surrounding sea floorsuch that normal abyssal plain sediments could not bedeposited on bathymetric highs. As terrigenous abyssalplain sedimentation continued to the north, it might bepostulated that subsidence of the area under discussioneventually brought the crest of the knoll within reach ofturbidity current sedimentation. The rather thick abyssalfan to the north and interpreted stratigraphic relationshipswithin the fan suggest that accelerated burial subsidenceprobably took place during Pleistocene time. Alterna-tively, the relationships described above could be inter-preted as an indication of eventual "filling" of thesoutheastern "end" of the abyssal plain, some knolls beingburied during earlier stages of sedimentation. Other knollsof greater relief still stand well above the level of theabyssal plain and are thus without a Pleistocene abyssalplain cover. The latter interpretation would be enhancedif it could be shown that a thin sequence of Pliocenepelagite occurs beneath the upper Pleistocene abyssalplain sediments in Site 96.

Although Core 1 is interpreted as representative ofMississippi abyssal plain sedimentation, it should bepointed out that considerable calcareous detritus ispresent, apparently concentrated in the fine fraction. Pa-leontological data suggests a preponderance of Upper

Cretaceous carbonate, indicating that considerableamounts of slumping from the Yucatan and/or Floridacontinental slope were probably occurring during LatePleistocene sedimentation. On the other hand, most of thethin silts and silty, very fine sands of Core 1 appear to behighly quartzose, which suggest a terrigenous source(Mississippi Fan). Low feldspar and high montmorillonitecontents also support a Mississippi Fan source.

Core 2 (Early Oligocene) contains the youngest strati-graphic occurrence of chert yet noted from the variousholes drilled on Leg 10. This tends to support the interpre-tation of a "silica gradient77 towards tne southeast as pos-tulated on the basis of results at Sites 86, 94, and 95. Thepresence of ash and siliceous organisms in Core 2 is alsosomewhat noteworthy since abundant ash in Oligocenesediments has not been noted previously from other holes.The lower cores (3, 4, and 5) appear quite similar butslightly less clayey or more calcite-rich as compared tocorrelative sediments in Sites 86, 94, and 95.

Physical Measurements

Natural gamma-ray measurements of Site 96 coresshow a marked contrast between Core 1 (high terrigenousclay content-high gamma count) and the remaining cores(low clay content). Core 2 has several zones yieldinghigher than normal counts which correspond to ash-richintervals. The lower Tertiary cores are quite comparable,in terms of gamma-ray count, to stratigraphically equiva-lent cores of Site 95. No gamma-ray data were obtainedfor Cores 4 and 5.

GRAPE bulk density is approximately the same forCores 1 and 2. Core 3 is too disturbed to yield meaningfulbulk density data and was omitted from the summarychart. Penetrometer data again reflected consolidation ofthe sediments with depth. Penetrometer measurements on

298

SITE 96

Cores 3 and 5 are based on fragments of chalk thought torepresent undisturbed sediment at those depths. In draw-ing the various curves on the summary chart, the interpre-tations previously discussed were used as a guide and, asa result, are highly interpretive.

BIOSTRATIGRAPHY

As interpreted from the fossil plankton (foraminifersand calcareous nannofossils), the biostratigraphy of Site96 is summarized in Figure 1. The section penetrated iscompressed (Late Paleocene to Holocene in less than 320meters), but it is not known whether it is condensed orshortened by a number of disconformities (probably thelatter). The Pleistocene core (10-96-1) apparently is asdiluted (with terrigenous clastic debris and residuum) asare glacial sections in the northwestern Gulf of Mexico.The allochthonous materials, however, seem generallymuch finer at Site 96 than in areas more directly affectedby the Mississippi River. Almost all of the reworked cal-careous nannofossils recovered from Core 1 are of LateCretaceous (probable Campanian) age, although there isa small component furnished from deep marine Miocenesediments.

Sample 1 (10-96-1, top of core):The assemblage from this sample is essentially the sameas that listed for Sample 2.

Age: Pleistocene (glacial), probably Nebraskan.Environment: Bathyal.Remarks: The dominant flora is a reworked Late Creta-ceous (probable Late Campanian) assemblage, essentiallyas listed for Sample 2 (10-96-1, CC).

Sample 2 (10-96-1, CC):Globorotalia truncatulinoides, Globigerinoides ruber(white), G. triloba, Globigerina sp. cf. G. inflata, G.eggeri, and G. bulloides.

Age: Early Pleistocene (glacial), probable Nebraskan.Environment: Bathyal.Remarks: The sample contains very common reworkedLate Cretaceous (probable late Campanian) calcareousnannofossil assemblage, including: Discoaster 1 hayi, Ark-hangehkiella cymbiformis, Vagalapilla octoradiata, Zygo-discus deflandrei, Micula staurophora, Prediscosphaeracretacea, Eiffelithus angustus, E. turriseiffeli, Watznaueriabamesae, Cretarhabdus conicus, and Microrhabdulus bel-gicus.

Sample 3 (10-96-2, CC):Globorotalia opima opima, G. nana, G. sp. cf. G.pseudokugleri, Globigerina angulisuturalis, G. ciperoen-sis, Globoquadrina venezuelana, Catapsydrax dissimilis,Cyclococcolithus neogammation, Reticulofenestra scis-sura, R. umbilica, Sphenolithus ciperoensis, S.pseudoradians, Helicopontosphaera parallela, H.seminulum ssp., H. truncata, Discoaster adamanteus,D. deflandrei, D. trinidadensis, and radiolarians of theDorcadospyris ateuchus zone.

Age: Early Oligocene (P. 21), the Globorotalia opimaopima Zone.Environment: Bathyal.

Sample 4 (10-96-3, CC):Globorotalia rex, G. aequa, G. gracilis, G. wilcoxensis,G. sp. cf. G. quetra, Globigerina sp. cf. G. soldadoensis,Chiasmolithus grandis, C. consuetus, C. Californicus,Cruciplacolithus tenuis, Heliorthus distentus, Fasciculi-thus involutus, Discoaster lenticularis, and radiolariansof the Bekoma bidarfensis zone.

Age: earliest Eocene (P. 6), the Globorotalia rex Zone.Environment: Bathyal

Sample 5 (10-96-4, CC):Globorotalia velascoensis, G. aequa, G. occlusa, G.acuta, Globigerina sp. cf. G. soldadoensis, Heliorthusdistentus, Zygodiscus sigmoides, Cruciplacolithustenuis, Fasciculithus typaniformis, F involutus, Eric-sonia alternans, Toweius sp., Marthasterites sp. aff. M.contortus, Chiasmolithus bidens, Ellipsolithus sp., andradiolarians Buryella tetradica n. sp., Hamptoniumpennatum n. sp., Phormocyrtis striata exquisita andPhormocyrtis turgida.

Age: Late Paleocene (P. 5), the Globorotalia velascoensisZone.Environment: Bathyal.Remarks: Several inches of chert were cored in the lowerpart of this barrel.

Sample 6 (10-96-5, CC):Globorotalia velascoensis, G. pseudomenardii, G. acuta,G. laevigata, G. aequa, Globigerina velascoensis, G. lina-perta, G. primitiva, G. triangularis, Chiasmolithus con-suetus, Cruciplacolithus tenuis, Toweius eminens,Fasciculithus typaniformis, F involutus, F. mitreus, F.sp., Coccolithus marisomontium, Ericsonia sp., Dis-coaster lenticularis, D. sp. cf. D. gemmeus, and radi-olarians Buryella tetradica, B. pentadica n. sp., andPhormocyrtis striata exquisita.

Age: Late Paleocene (P. 4), Globorotalia pseudomenardiiZone.Environment: Bathyal.Remarks: Most of the foraminifers contained in the sam-ple examined were Pliocene to Holocene contaminants.

DISCUSSION AND INTERPRETATION

Originally, the knoll at the mouth of Catoche Tongue(Site 96) was thought to be an igneous intrusion. This idearesulted from examinations of other such features in thearea and the magnetic anomalies associated with them.However, a very brief survey of the site indicated that nomagnetic anomaly existed for the knoll in question. Auniform magnetic field apparently exists in the area. Thiswas a surprise and now casts doubts as to the assumedorigin of the structure.

While Glomar Challenger was on Site 96 (Figure 2),March 30-31, 1970, five cores were recovered between thesea floor and a subbottom depth of 332 meters (Table 1).Upper Paleocene sediments were the oldest recovered. NoPliocene or Miocene sediments were recovered, nor did werealize the objective set for Site 96. No indication of thenature the core of the diapiric structure drilled was ob-tained due to premature site abandonment resulting frombeacon failure.

299

SITE 96

SITE 96 WATER DEPTH 3540 METERS

RELATIVEAGE

APPROXIMATEYEARS

(MILLIONS)

ZONESAND

SUBZONESRADIOLARIAN

ZONES

SUBSURFACEDEPTH

(METERS)

COREAND

INTERVAL

EARLY

Iδ

I δ

Io2.2

50

Globorotaliatosaensis

100 101

EARLY 29

EARLY

LATE

150

200 199-

250

52

56

Globorotaliarex

Gr. velascoensis

Gr. pseudomenardii

Bekoma300

3 0 1

bidarfensis

V////////Å 321

Figure 1. Biostratigraphic summary of Site 96.

300

2 -

SITE 96

800 £cse 124°8 o

2000:fms

η

Figure 2. Profile record, Site 96.

Core 1 is comprised of a rather thick sequence of Pleis-tocene laminite terrigenous silts/clays and associatedquartzose turbidites overlying a thick sequence of lowerTertiary coccolith ooze and chalk which include an occa-sional chert layer. Plant debris is common to abundant.Most of the sections contain traces to rare amounts ofabraided dolomite rhombs. The carbonate content aver-ages about 35 per cent; detrital carbonate is the mainconstituent. The carbonate content reflects the rather slowrates of deposition as compared to the Mississippi Fan andthe Sigsbee Abyssal Plain sediments. Since much of thecarbonate debris present consists of Upper Cretaceouscarbonates, the Campeche Bank was the probable sourceand slumping the probable transporting mechanism of agood portion of the sediments recovered. Other constitu-ents found are siliceous skeletal material and volcanicglass.

The occurrence of very fine sand turbidites on top ofthe knoll suggests that either turbidity currents can carryfine sand-sized sediments in suspensions 16 or more me-ters above the sea floor or that the relief of the knoll wasless than at present.

Core 2 (199-208 meters), of Late Oligocene age, is acalcareous foraminiferal nannofossil pelagic ooze with av-erage carbonate content of about 85 per cent Radiolarians,

siliceous sponge spicules, quartz, and amphibole-bearingheavy minerals are present.

The sediments of Core 3 (301-310 meters), of EarlyEocene age, are silica-rich organic oozes. Radiolarians areabundant and siliceous sponge spicules common to abun-dant. The carbonate content averages about 50 per centand is in the form of calcareous nannofossils and forami-nifers. Dolomite rhombs are also present. The first appear-ance of soft chalk occurs in Core 3. Calcareous chert ofgreenish gray color in Core 3 represents the youngeststratigraphic occurrence of chert yet noted in the Gulf.

Core 4 sediments are Upper Paleocene nannofossiloozes containing mainly calcareous nannofossils, dolo-mite, chert, traces of foraminifers, radiolarians, and vol-canic glass.

The presence of lower Tertiary pelagic oozes in Site 96suggests that the knoll formerly was elevated above the seafloor. Subsequent subsidence of the knoll or upbuilding ofthe surrounding sediments could have brought the crest ofthe knoll within the reach of turbidity currents during theLate Pleistocene. Alternatively, the level of the surround-ing abyssal plain may have risen to bury the knoll to sucha depth that turbidites could reach the upper parts of theknoll.

301

SITE 96

The average rates of deposition at Site 96 weredetermined to the the following:

Late Pleistocene 5.6 cm/103 yLate Oligocene to Early Pleistocene 0.33 cm/103yEocene 0.42cm/103yLate Paleocene to present 0.6 cm/103y.

As one can see, the rates of deposition are rather low; thesection penetrated is compressed, being either condensedor shortened by a number of disconformities. However,the average rate of deposition for the site is similar to thatfound at Sites 86, 94, and 95, all located on topographichighs.

In general, the main objective of the hole was not real-ized due to failure of the beacon and the shortage of time.It is unfortunate that the hole was not drilled to comple-tion, particularly since no magnetic anomaly exists over

the knoll. Data of the U.S.S. Kane, Lamont-Doherty, andTexas A & M will be reexamined to determine the mag-netic nature of the structure and, thus, the most likelyexplanation for its origin.

REFERENCES

Bryant, W.R., Meyerhoff, A.A., Brown, N.K., Furrer, M.A.,Pyle, T.E. and Antoine, J.W., 1969. Escarpments, reef trends,and diapiric structures, eastern Gulf of Mexico. Bull. Am.Assoc. Petrol Geologists. S3 (12), 2506.

Gough, D.I., 1967. Magnetic anomalies and crustal structure ineastern Gulf of Mexico. Bull. Am. Assoc. Petrol. Geologists.51, 200.

Pyle, T.E., Antoine, J.W., Fahlquist, D.A. and Bryant, W.R.,1969. Magnetic anomalies in Straits of Florida. Bull. Am.Assoc. Petrol. Geologists. 53 (12), 2501.

302

SITE 96

SITE 96

AGE DEPTH LITHOLOGY

— 100 r.

— 200 :.S

— 300

-400

1 4 i

LITHOLOGIC DESCRIPTION

1: Olive-gray to dark o l i ve-gray CLAY.

2: Very l i gh t greenish-whiteFORAM NANNO OOZE, loca l lyCHERT-bearing with somethin ashy zones.

3: Light greenish-white FORAMNANNO CHALK (so f t ) .

4: As above, but very l i g h tgreenish-white toyellowish-white withcalcareous greenish-grayCHERT.

5: Very l i g h t yel lowish-white FORAM NANNO CHALK(soft).

POROSITY

100I

4.0

PENETROMETER

cm

2 . 0 0 . 0I I

1.01

DENSITYg/cc

2.0I

3.0 13.0

2 NATURAL GAMMA10 counts/75 sec

25.0 37.0I I

49 .0I

-3.

304

o

Site 96 Hole Core 1 Cored Interval: 101-110 m

g 1? GRAIN SIZE

p: 3 WEIGHT %

> al en o I " I

S S ^ aü LITHOLOGY ë 5 LITHOLOGIC DESCRIPTION I £ d

0.5 -1 I VOID

1.0-- Brecciated-mechanically disturbed.

- I-I-I-I-I-I-I- ^ 5Y3/1 to mixed 5Y3/1 and 5Y4/1 .

- ̂ ^ = ^ 5 5Y3/1

1 - <?_-_=_2-=^• - 0.0 18.3 81.7

~iHH?!HH3^ SY4/1 dominant with coarser zones of 5Y3/1 .

- :-I-ZjHHHK

£ ~ "-I-I-I-I-I-I-• CLAYIU _.-_-_-_-_-_-_-! i O l i ve gray to dark o l i v e gray; massive toS? --ZHHHHHH: I — rarely to occasionally laminated; 0.1 15.884.2>- ~ 3^_-_-_3£Hr- occasional graded clayey s i l t laminae anda. _ .-_-_-_-_-_-_:: I rare graded beds of very fine sand2 ~ -_-_-_-i_-̂ rzrzr I (quartzose).

4 - :-I-I-»I-£H i

I -I-I-I-I-C-I-I- I

- -I-I-I-I=I-I-I- I - 0.012.4 87.6

: E=iSθE=i=z= I

^ ^-I-I-I-I-I-: ' - 0.014.3 85.7

- rz^r^z^zi Graded sandy si l t .

I z-~-i-iHHi-i-; I

— I — Z ^ i ! ! ^ ^ L ! -VOID

Core EH>I-I-I-Z-I-i

Catcher JHHHHH~

Site 96 Hole Core 2 Cored Interval: 199-208 m

§ | GRAIN SIZEP « WEIGHT %

Su. ë . .L U I — UJ ox; Q i — > -

S S K S LITHOLOGY S 5 LITHOLOGIC DESCRIPTION I d d

I _ —H^ 1 - _ Mechanically disturbed throughout. 53 50.143.6

I r^JT+^+IT^I FORAM NANNO OOZEZ^T ~^i~TTT, V e r y ] 9ht greenish-whi te (N9-5G9/1- JCJ=^ZȱJ, *Tcto _ stained with N6); vague laminae/burrow ,. „ . . . ,- 1 % ! ^ f i l l , probably s t rong ly (?) burrowed; s * ^Ö ' 1 4 0 - 6

~ ~ ^ ~ ~ i ~ 1 " |~ cher t -bear ing and ashy loca l l y -based on- — 1 — — i — - garnna count and smear s l i d e s .

- ^ \ ^ • I' /HH^s-_

Z u i ^ X i S ^ ~ 10.153.736.2Z. ~ —' —H7^ As above. Strongly streaked with N7 and- ~ i ~ 1 " ! ^ " N3 fecal stain.

2 — ~| ~1 1 * As above with:

ü I^-VT^V CHERT- _ Greenish-gray (5G6/1, mottled with 5G8/1-

— —1—' — 1 — ' - 9/1); calcareous.

= = ^ ^ EIl^I+rt - 4.2 50.145.6

~ ~ + ~ | ~ l ~ |~ Scattered chert fragments.

I-'—I—1 - - 4 6 50.844.6

' — H ^ ^ - L Z AS above. Less d i s tu rbed .

Core — |—t— | — I — ICatcher — — 1 — —>—

£2HW

oON

Site 96 Hole Core 3 Cored Interval: 301-310 m

§ i GRAIN SIZE

P S WEIGHT %§ co S . _ ^ _ _ _ _ _»— α: et; o 1 1

S S £ £ LITHOLOGY α 5 LITH0L0GIC DESCRIPTION I £ d

- t

I = ^ = = - j

- ' I ' I ' I ' Mechanically disturbed throughout.

- . i ! i ! 110.5-1 . I I I H

-1 ' i ' i ' i1 - ' ) ' i ' | I1 _ L1 I ' i π

- I I j+η

Z h l ' J I j-f- FORAM NANNO CHALK ( s o f t )- I I l-j-4 Light greenish-white (5G9/1 mottled with

| | i N7); strongly burrowed. Scattered pieces- I . I [+-j• of soft chalk throughout.

- d i ' i I i

- ' I ' I ' I-

-– I I I

I I I I

- I ) I i Llf

- I , I . t-r - 4.9 45.949.2- I ' I Ni

- ' ' '

LU _ —| ) 1

o _ I I ( I , 4-

i ε — E ! ^

^ - T ' i ' i ' - 5.9 44.949.2= j l l l

- - j - I j I j I

I ± - f . ' 1 I 4! - 5.2 39.355.5I I . I . I

- I • I -\—r As above. Very rare vague laminae.

if^T- T ' 1 ' i-L - 4.4 45.250.3- I |-H-

- ' 1 ' 1 1 1=

- ' ' '- ' ' 'I 1 I 1 I '

Core 1 I 1 I 1 +

C a t c h e r , 1 . 1 . - +

I I I I ! 1 ' 1 I i l I I I I I

Site 96 Hole Core 4 Cored Interval: 321-329 m

§ != GRAIN SIZE

P < WEIGHT %

O t/) 21

<- cc cc o I I

UJ 1— UJ o πz Q i — >-

< S « ë LITHOLOGY Q 5 LITHOLOGIC DESCRIPTION 5 L̂ 3

UJ l A I . I j - 1

5 ^ Core 1 j 1 I 1 H C o r e c a t c h e r :

o °- Catcher | j I ] | A pg ' ! ! FORAM NANNO CHALK (sof t )^ Very l i g h t greenish-white to l i g h t

yellowish white-1 and

1 CHERTGreenish-gray 5GY5/1. Calcareous(impure).

Site 96 Hole Core 5 Cored Interval: 329-332 m

§ §! GRAIN SIZE

P < WEIGHT %

^ g 2 ° ÜTΠTΠT^ S S £ LITHOLOGY ë 5 LITHOLOGIC DESCRIPTION I L̂ d

~ I '1 ' I T Mechanically disturbed in part.

II ' I ' I '

° 5 ~ I . I -j-f-r- FORAM NANNO CHALK ( s o f t )z 1 - I I | ^p Very l ight yellowish/white (5Y9/1-N9);ö J~^ j ' j strongly burrow-mottled.

ë 1 -^JH=JT±_i 1 ' 1 ' 1 HLZ

1 1 ' 1 ' 1

Core I I ' I HZ1 1 1 1 ' 1

Catcher 1 ' 1 ' i~?Z

I I 1 ; 1 1 1 ! i - l 1 I I 1 I

HW

ON

WET-BULK DENSITY, gm/cc

1 2 31 1 i i i I i i i i i i i i « i i ' i i

POROSITY,*TOO 0

GrainDensity-32 o

1 , E M3 3 σ> Q _

CMrθ

1 -

2 -

3 -

4 -

5 -

6 -

7 -

8 -

9- 1

-25

-50

-75

- 1 0 0

-125

1—150

SITE 96

96-1-1 96-1-2 96-1-3 96-1-4 96-1-5 96-1-6

307

SITE 96

WET-BULK DENSITY, gm/cc

1 2 3

POROSITY,* GrainDensity-3 2 o

MOn

1 -

2 -

3 -

5 -

6 -

7 -

8 -

CM

ro

-25

-50

-75

-TOO

-125

1—150 rt|||

96-2-1 96-2-2 96-2-3 96-2-4 96-2-5 96-2-6

308

SITE 96

WET-BULK DENSITY, gm/cc

1 2 3| i i i M ' ' ' ' I ' ' ' ' I i ' > « I

POROSITY, %100 0

GrainDensity

2 o

MO-i

9-1

CM

ro

U I

L

hioo

hl25

1—150

96-3-1 96-3-2 96-3-4 96-3-5 96-3-6

309

SITE 96

WET-BULK DENSITY, gm/cc

1 2 3

POROSITY,*100 0

π i i l l

GrainDensity

.1 °I3R M

ü-i

CM

1 --25

2 -

3 -

4 -

5-

-50

-75

6-- 1 0 0

7 -

9- 1

-125

1—150 w

96-5-1

310