3. SITE 219
The Shipboard Scientific Party1
With Additional Reports From
Norman Hamilton, University of Southampton, United Kingdom
Johannes Hunziker, Mineralogisch-petrographisches Institut der Universitàt, Bern, SwitzerlandandPaleontological Laboratories of the Geological Survey of India
SITE SUMMARY

Early

Early

70

75C

Early

Figure 1. Position of Site 219 and adjacent Leg 23 sites(shown by +). Contours at 200, 1000, and 4000 meters,from Laugh ton et al. (1971).
SITE DATA
Dates: 1315 10 Mar-1945 13 Mar 72
Time: 78 hours
Holes Drilled: 2;
Position (Figure 1): 9°01.75 N, 7 2 ° 5 2 . Ó 7 ' E
Water Depth by Echo Sounder: 1764 corr. meters
Total Penetration: 411 meters
Total Core Recovered: 223.1 meters from 42 cores
Age of Oldest Sediment: Late Paleocene
Basement: Unknown

Early

ABSTRACT
Shallow-water Upper Paleocene limestones, sandstones,
and siltstones are succeeded by Eocene chalk and ooze. The
sea bed began to sink about 2000 meters in Early Eocene
times. Biogenic silica, sometimes as chert, is common in the
Eocene. Sedimentation was at a minimum in the Oligocene.
Mainly detrital silty clay nanno ooze was laid down in
post-Early Miocene times. Upwelling began in the Middle
Miocene and continues today. Volcanic glass is found in the
Pleistocene.
Robert B. Whitmarsh, National Institute of Oceanography,
Wormley, Godalming, Surrey, United Kingdom; Oscar E. Weser,
Scripps Institution of Oceanography, La Jolla, California: Syed Ali,
State University of New York, Stony Brook, New York; Joseph E.
Boudreaux, Texaco, Inc., New Orleans, Louisiana; Robert L.
Fleisher, University of Southern California, Los Angeles, California;
Dan Jipa, M.I.M.G. Institutul Geologic, Bucharest, Romania; Robert
B. Kidd, Southampton University, Southampton, United Kingdom(Present address: National Institute of Oceanography, Wormley,

Godalming, Surrey, United Kingdom); Tapas K. Mallik, Geological
Survey of India, Calcutta, India; Albert Matter, Geologisches
Institut, Universitàt Bern, Bern, Switzerland; Catherine Nigrini,
Lexington, Massachusetts; Hassan N. Siddiquie, Geological Surveyof India, Calcutta India (Present address: National Institute of
Oceanography, Goa, India); Peter Stoffers, Laboratorium fur
Sedimentforschung, Universitàt Heidelberg, Heidelberg, Germany.
35

SITE 219
BACKGROUND AND OBJECTIVES

Site 219 is located on the crest of the Laccadive-Chagos
Ridge (Figure 1). This ridge is a major linear feature of thefloor of the Indian Ocean. Its origin has been said, evenrecently, to be both oceanic and continental by different
authors. The almost complete lack of samples from theridge, other than surficial sediments, has prevented detailed
study of its history and nature. Thus a drill hole was clearly
desirable but, although the ridge is a feature probably
deserving half a dozen holes, time was only allotted for one
reconnaissance hole on the northern part of the ridge.
During Leg 24, a second hole was drilled near the Chagos
Islands. The Laccadive-Chagos Ridge extends a distance of2200 km in a north-south direction, from the Chagos
Islands at 6°S to the Laccadive Islands at 14°N. The ridge isslightly arcuate, being concave to the west. A considerable
length of the crest of the ridge is composed of shoals,
banks, and coral reefs at depths less than 1500 meters, and,broadly, these shoal areas are grouped as the Laccadive,
Maldive, and Chagos islands. Between the shoals, the water
depth is commonly around 2000 meters and, exceptionally,reaches 4000 meters between the Maldive and Chagos
islands. To the west of the ridge, the sea floor everywhere isrelatively steep at first and then flattens out at around 4000
meters. The east flank is modified by the proximity of the
Indian continental slope and abutting abyssal plain
sediments at 2500 meters depth north of 3°N, but south ofthe equator a scarp is developed, which drops down to atleast 4500 meters, with a parallel ridge and trough (theChagos Trench) flanking the Chagos mass (informationfrom unpublished charts prepared for the International
Indian Ocean Expedition [IIOE] Atlas by R. L. Fisher and
A. S. Laugh ton).
Before the drilling by Glomar Challenger, no sedimentary rock, other than coral rock and associated detritus,
was known to have been obtained from anywhere along thewhole length of the Laccadive-Chagos Ridge (Wilson,
1963). A single sample of a glassy basalt from the west
flank of the Laccadive Islands (11°18'N, 71°00'E) has beenreported by Vinogradov et al. (1969).
Probably the earliest geophysical measurements made on
the ridge were the pendulum gravity observations of
Glennie (1936) in the Maldive Islands. He found large
negative isostatic anomalies (about -75 mgal) which heinterpreted in two ways. First, if the anomalies are due tolocal superficial anomalies of density, such as a considerable
thickness of coral rock, then the Maldive Islands "mark theoriginal site of an oceanic ridge, not a continental block,which has since sunk down under isostatic adjustment." A
second hypothesis proposed that the Maldives could lie
over "an area where a block of sial has subsided as a resultof the downwarping of the lower crustal layers." Glennie
calculated coral thicknesses on the basis of thesehypotheses, but his figures must be tempered by the factthat he used the Helmert gravity formula of 1901, not the1930 formula which yields larger negative anomalies. On
the other hand, the former gives a gravity value at thislatitude which differs little from the newly adopted 1967
gravity formula (Woollard, 1969). In addition, however,account should be taken of the large regional negative
free-air anomaly in this part of the Indian Ocean, recently
discovered from satellite observations (Gaposchkin and36

Lambeck, 1971). This anomaly is about -60 mgal in theMaldive area, suggesting that the isostatic anomaly, if any,
attributable to the sinking of the Maldive Islands is far lessthan Glennie supposed.
Magnetic observations by ships during the IIOE haveshown that substantial magnetic anomalies (Figure 2),
several hundred gammas in amplitude and with wavelengthsof tens of kilometers, exist along tracks passing through the
Laccadive and Maldive islands (D. H. Matthews, unpublished IIOE Atlas charts; Admiralty Hydrographic Office,1963 and 1966). These observations led to wide acceptanceby oceanographers that the Laccadive-Chagos Ridge has abasaltic and, therefore, probably oceanic foundation.
This conclusion has been borne out by the crustal
velocities of 4.8 to 6.1 km/sec and 6.7 to 7.1 km/sec foundby seismic refraction studies over the Ridge at latitudes
9°N, 2°S, and 5%°S (Francis and Shor, 1966). However,
only at the northernmost station, situated very close to Site
219, was an upper mantle velocity detected, and thisunreversed line indicated a crustal thickness of 17.5 km. At
2°S, the Moho is probably at least 20 km deep. Thus,
Francis and Shor indicate that the depth at which a normal
upper mantle velocity is reached beneath the LaccadiveChagos Ridge is comparable with that close to Eniwetok
Atoll, the inference being that the Maldive Islands rest on a
subsided volcanic foundation. Before Leg 23, only fiveseismic reflection profiles which crossed the northern partof the ridge were available (Ewing et al., 1969; Harbison

WESTSOUTHWEST^^____^-v/^^

NO DATA

-

1000

-

2000

Figure 2. Bathymetric and magnetic profiles across thenorthern part of the Laccadive-Chagos Ridge obtainedby H.M.S. Owen (Admiralty Hydrographic Office 1963).
The profiles are arranged in order of decreasing latitude
from top to bottom. Site 219 is situated between the
two topmost profiles.

WEST

LO
-J

Figure 3. Two seismic reflection profiles (CD and EF) across the northern end of the Laccadive-Chagos Ridge (courtesy ofN.O.A.A. Atlantic Oceanographic andMeteorlogical Laboratories, Miami). The arrow on profile EF marks the proposed site. For tracks of these and other available profiles see inset profiles AB
CD, EF from Oceanographer, 1967; profile GH from Vema-19, 1963; profile IJ from Conrad-9, 1965.

SITE 219

and Bassinger, 1973), and three of these were close together
within the channel between the Laccadive and Maldive
islands (Figure 3 inset). Due to the absence of any presite
survey, these profiles, therefore, were the sole data fromwhich a proposed site could be chosen. In general, all the
profiles, except the northernmost one (profile AB, Figure 3
inset), show a sea bed over the ridge which varies fromsmooth to hummocky. It has a layer of transparent
sediment usually at least 0.4 sec thick, overlying anirregular and probably faulted acoustic basement. In places,
the basement crops out. Profile AB apparently has eventhicker sediments which include turbidites, and the basement
does not crop out but is only clearly seen at one point. The
JOIDES Indian Ocean Panel had made a preliminary
suggestion for a site in the general area of profile AB. In
view of the above comments, however, and the possible
complication of being rather close to the Indian continental
margin, a site farther south was sought. The proposed site
was located on the sediment covered west slope of abasement outcrop forming the crest of the ridge which isbounded by a 1100-meter scarp to the east (profile EF). A
similar outcrop exists on profile CD, and it has beensuggested by Harbison and Bassinger (1973) that together
they form part of a basement ridge extending from 9°N to
20°N. The proposed site seemed to offer the best chance ofsampling the acoustic basement in a region near the crest of
the northern part of the Laccadive-Chagos Ridge and had
the additional advantage of control from a nearby seismic
refraction station (Francis and Shor, 1966).
The objectives of drilling the site were thus to:1) Determine the nature of the true igneous foundationof the ridge and date it if possible.
2) Determine the history of the site from the sediments,and3) Obtain samples for paleomagnetic measurements
ashore.
The JOIDES Advisory Panel on Pollution Prevention and
Safety set the operational constraint that minimum coring
requirements should be alternate coring and drilling.
OPERATIONS

Site 219 was approached from the east at 10 knots. At a
distance of about 20 km from the proposed site, speed was
reduced to 8 knots in order to improve the clarity of
the airgun records during the presite survey. Glomar
Challenger1 $> track passed up to 7 km to the south of the
profile EF (Figure 3) obtained by Oceanographer andshowed the same transparent layer overlying an irregular
diffuse reflector. An east-facing fault scarp was initiallycrossed at 1505 hours. After a further 55 minutes, the shipturned north and then east to obtain an additional crossingof the fault scarp so as to determine its trend. Immediately
after the second crossing of the scarp, Glomar Challenger
turned to starboard onto a westerly course and reduced
speed to 5 knots. A 13.5 kHz beacon was dropped under
way at 1819 hours, AVi hours after the ship had reduced
speed to 8 knots for the site approach. Immediately after
the towed gear had been brought onboard, the ship
returned to the beacon to take up station.
A program of nearly continuous coring was planned.
This resulted in the taking of 42 cores and the drilling of
only 44 meters of sediment in two holes (Table 1).
38

The soft pelagic sediments on the sea floor were easily
penetrated and the first 13 cores, spanning the interval 8 to
127 meters, were continuously cored. A punch core wastaken at the surface to minimize sediment deformation.
The somewhat more indurated chalks occurring between
127 and 210 meters were not as easily penetrated, andcirculation was broken several times.
At Hole 219, some difficulties were encountered
between 210 and 273 meters. Hard layers consisting mostlyof chert alternated with softer material, including sands.
Recovery of the softer material was poor as circulation had
to be broken frequently. The inner barrel of the final core(Core 28) became stuck and the drillers were unable toeffect circulation suggesting that the water jets in the bit
were plugged. The drill string then had to be tripped backto the surface, terminating operations at this hole. The
inner barrel was found to be stuck and the jets filled with aforaminifera sand, which apparently came from farther up
the hole.
An offset of 200 feet to the east was made for Hole
219A and, to hopefully avoid the running sand found at theprevious hole, it was drilled down to 290 meters or 17
meters below the bottom of the previous hole. One
hundred barrels of mud were also spotted in the hole. The
drill string was run with the inner core barrel in place
during this operation, resulting in the recovery of 5.1
meters of sediment of unknown stratigraphic position inCore 1. Core 2 recovered no sediments and the drill string
became temporarily stuck again, probably due to therunning sands from farther up the hole.
Cores 3 to 14 encountered well-indurated sediments andbit weight had to be increased considerably. Also, the water
pump was operated continuously throughout the coring
operation. Fortunately, however, there were few, if any,
soft sediment streaks, and core recovery was good. The
penetration rate decreased as the sediments became
progressively harder, and it was finally decided to abandon
Hole 219A at a depth' of 411 meters. When the bit was
brought on deck the teeth showed practically no wear andthe bearings were only slightly worn.
Glomar Challenger departed from Hole 219A at 0009
hours on March 14 in a northerly direction at 5 knots while
the airguns and hydrophones were streamed. At a distanceof about 2 km from the beacon the ship turned to port totake up a southerly course so as to pass over the beacon.
The beacon was passed at a range of about 200
meters. Five minutes later the ship came up to full speed
and began its passage track to Site 220 via a point at
8°15'N, 72°56'E. The purpose of this slight deviation fromthe direct track was to obtain a north-south profile acrosspart of the Nine Degree Channel and thus obtain acontinuous seismic section from an atoll into the deep
water to the west and also to twice cross the projected
trend of the NNE fault scarp seen 9 km to the east of Site
219.
A bathymetric chart was constructed of the area around
Site 219 from the above site survey and from the collectedsoundings of other ships (Figure 4).
LITHOLOGY

Two holes (219 and 219A) were drilled at Site 219. The
first hole was drilled down to 273 meters. A second hole,SITE 219
TABLE 1TABLE 1
Coring Summary, Site 219

Core

Date/Time
Core on Deck
(Time Zone-5)Depth Below
Sea Floor

(m)

Cored
(m)

Recovered(m)Hole 219

ia
2
3

4
5
6
7
8
9
10

11
12b
13^
14d
15

16
17
18
19
20
2ie
22
23
24f

25
26

27
288

11 Mar:
0030
0250
0330
0415
0500
0545
0630
0715
0800
0845
0930
1035
1150
1250
1350
1450
1550
1620
1715
1810
1930
2040
2220
2330
12 Mar:
0015
0130
0220
1000

0-6
6-15
15-24
24-33
33-42
42-51
51-60
60-69
69-78
78-82
82-91
91-100119-128128-137
156-165
165-174
174-183
183-192
192-201
201-210210-219219-228228-237237-246

6.0
9.0
9.0
9.0
9.0
9.0
9.0
9.0
9.0
4.0
9.0
9.0
9.0
9.0
9.0
9.0
9.0
9.0
9.0
9.0
9.0
9.0
9.0
9.0

246-255
255-264264-273273-273
Totals

9.0
9.0
9.0
0.0
235.0

0.5
1.5
3.9
cc
172.5

0-290
290-299299-308

9.0
9.0

5.1
0.0
2.2

308-317317-326326-335
335-344344-353353-362362-371371-380
380-387387-396402-411
Totals

9.0
9.0
9.0
9.0
9.0
9.0
9.0
9.0
7.0
9.0
9.0
115.0

4.7
2.0
2.4
3.6
6.8
6.2
3.9
4.3
6.3
2.2
6.0
50.6

5.6
7.3
5.5
8.2

4.4
9.0
8.0
7.8
8.8
9.3
8.8
8.6
9.0
8.4
9.4
9.0
7.5
9.3
9.4
8.0
5.3

CC

cc
CC

Hole 219A

lh
2i
3

4
5
6
7
8
9

10J
11
12
13
14k
a

12 Mar:
2105
2210
2320
13 Mar:
0040
0130
0225
0345
0500
0610
0900
1055
1345
1600
1900

Punch core, 2 inch liner.
b Rotating at 20 r.p.m. (at least) from here on.
cDrilled 19m with core barrel in place.
d Broke circulation for first time.
e
Cut in 30 mins, previously 4 to 12 mins.
f Spotted mud before coring.

footnotes continued

g Bit and core barrel stuck.
nCore collected while drilling 290m, spotted mud before
retrieving core.
1
Pipe and core barrel stuck temporarily.
J Coring time 1-2 hours from here on.
k Spotted mud before coring.

219A, was drilled to a depth of 411 meters. The first hole,
excepting for several small intervals, was continuously
cored down to 273 meters. Hole 219A was washed down to
290 meters and then cored continuously from 290 to 411
meters.
Five lithologic units were recognized. These are shownin Table 2.
Unit IThe entire upper part of this unit consists of detrital
silty clay nanno ooze which, with decreasing detritalcontent, becomes a detrital silty clay-rich nanno ooze in thelower part. The detrital percentage varies from 20 to 35
while nannofossils are more than 55 percent and calcium
carbonate ranges from 52 to 76 percent. The upper 15
meters, and the lower 30 meters, are foraminifera rich(about 15%). Volcanic glass, apparently fresh, is common as
disseminated grains in the upper 35 meters but does notexceed 5 percent. The sediments are varied shades of grayexcept for a thin olive-brown bed in Core 1, Section 3, 130
to 150 cm. The percentage of organic carbon (0.2% to0.3%) is relatively high in this unit.
Unit II

This unit is characterized by nanno-rich foram chalk andooze in the upper part and foram chalk and ooze in thelower part, all of which are white in color. In the upper
part, the percentage of nannofossils varies from 5 to 40
while that of foraminifera is from 60 to 95, and in thelower part, the foraminifera vary from 90 to 98 percent.
The calcium carbonate varies from 86 to 98 percent. The
alternating ooze and chalk layers are a few decimeters
thick. The change in lithology from unit I to unit II ismarked by a fairly abrupt color change from gray to white,by the almost complete absence of detrital minerals, as well
as by a sudden increase in foraminifera. Chalk was first
cored in this unit.
Unit III

This 73-meter unit consists of white oozes and chalkwhich contain some thin chert beds. The upper part ischaracterized by about 92 percent calcium carbonate, themiddle part by 84 to 87 percent and the lower part by 71
to 72 percent. Lithologically, the unit can be subdivided
into four subunits.
Subunit Ilia is characterized by foram nanno ooze andchalk which is locally zeolite bearing. Nannofossils
constitute up to 65 percent and forams to about 13 to 35
percent of the sediments. Minor amounts of micarb firstoccur in this subunit.
Subunit Hlb is a foram-rich nanno micarb ooze andchalk. As the sediment name indicates, micarb particles are
the dominant constituent.

39

SITE 219

72°30'

73°E

Figure 4. Bathymetric chart of the area around Site 219 with the tracks of Glomar Challenger and Oceanographer. Contour
interval lOOfms, depths in corrected fathoms, dots represent soundings by other vessels.
Subunit Ule consists of rad-rich micarb nanno ooze andchalk. Minor glauconite-bearing intervals also occur. In theupper portion of this subunit, the composition is asfollows: foraminifera (5% to 25%), micarb (20% to 65%),
nannofossils (15% to 60%), zeolite (trace to 10%),
Radiolaria (5% to 20%), and sponge spicules (2% to 8%).
Both the radiolarians and sponge spicules increase towards
the lower portion of the subunit. A decrease in siliceousorganisms from 15 to 5 percent between Core 19, Section 5
and Core 19, Section 6 is accompanied by chert formationand development of up to 8 percent zeolites. The chert
intervals are thin and only occur sporadically.
Subunit Uid consists of nanno-rich rad micarb ooze andchalk and also chert. Cherts appear at the bottom of Core19; below this there are many thin layers of chert. These
coupled with the presence of abundant radiolarians givethe entire interval a highly siliceous aspect. Nannofossils
range from 15 to 20 percent, Radiolaria, 20 to 25 percent,micarb, 40 to 55 percent, and sponge spicules and forams,
about 5 percent each.
The chalk and ooze intervals occur in roughly equalamounts in alternating intervals a few centimeters to ameter thick.
Unit IV
The recovery in the unit was poor, but both hard andsoft intervals were recovered. The hard streaks consist of40

thin yellowish-green chert and limestone. The softer
sediments, which are more prevalent, consist of nannoooze, foram chalk, micarb foram ooze and chalk, andzeolite micarb-rich foram chalk, Larger foraminifera areparticularly abundant, and they, having the properties of a"running sand," were probably responsible for the drill pipe
sticking and subsequent abandonment of Hole 219. No
doubt the largely unrecovered sediment from this unit
consists of the softer sediment washed away during drillingof the hard streaks. Some phosphorite concretions were
found in Core 26 of this unit. Electron microscope studies
of a sample from 24, CC reveal the presence of cristobalite
spherules.
Hole 219A, Core 1 represents material which accumulated in an open core barrel as the bit was washed down to
290 meters. Consequently, this melange of nondiagnostic
material is not part of the unit description nor is it
represented on the Site Summary.

UnitV
Subunit Va (the top 27 m) consists of grayish-yellow tograyish-green limestone. Much of the sequence is glauconite
rich or glauconite bearing. The calcium carbonate content
varies from 73 to 86 percent. The limestone contains foraminiferal and molluscan shell fragments. Some intervals show
burrow structure and parallel and cross-laminations.

SITE 219
TABLE 2
Lithologic Summary, Site 219

Thickness(m)

Subbottom
Depth
(m)

Cores

120

0-120

1-13

Ca. 26120-146

13-14

a White FORAM NANNOOOZE and CHALK.

19 >146-219

15-21

t> White FORAM-RICH
NANNO MICARB OOZEand CHALK.

13

c

26

219-300

22-27
1A-2A

300-411

3A-14A

Lithology
Units
I

II
Ill

Light gray, greenish-gray
DETRITAL SILTY CLAY NANNOOOZE. The upper and lower
portions are foram-rich.
White FORAM OOZE and CHALK,
nanno-rich in upper part.
White OOZES and CHALKS
containing nannos, forams,
rads and micarb in varying
proportions.

Subunits

White RAD-RICH
MICARB NANNO OOZEand CHALK.

> 73

d White NANNO-RICH
RAD MICARB OOZEand CHALK. Also
CHERT layers.
IV

V

Grayish-yellow to yellowbrown MICARB CHALK and
OOZE, LIMESTONE and CHERT.
Green and black LIMESTONE,SANDSTONE and SILTSTONE.

81aGrayish-green
LIMESTONE, GLAUCONITEBEARING or GLAUCONITERICH.

b Yellowish-green tograyish-green and darkgray CALCAREOUS
CEMENTED SANDSTONE,
SILTSTONE and CLAYEY
SILTSTONE. Gray togreenish-black CLAYEY
SILTSTONE and SILTYSANDSTONE.

27'
* IU
84.

Note: Only sediment names are capitalized.

Subunit Vb is dominated by terrigenous sediments
consisting of yellowish-green to grayish-green and dark graysiltstone, clayey siltstone, grayish- to greenish-black clayey
siltstone, and silty sandstone. Near the top is a 17-meterinterval of calcareous cemented glauconitic sandstonewhich appears to be transitional between subunits Va and
Vb. Some sediment layers are rich in shell fragments
including pelecypods, foraminifera, ostracods, red algae,
and bryozoans, which gives the interval a calcareous aspectin places. The calcium carbonate in this subunit ranges from
1 to 58 percent. The sequence is mostly well indurated or
cemented, locally laced by calcite veins (0.2 to 0.5 m thick)and in places strongly bioturbated. Some beds are welllaminated, and sandstone beds near the base of this subunit
show graded bedding as well as load casts and convolutebedding. Glauconite occurs in some of the intervals.
Due to limited space, the tables of grain size,
carbon-carbonate, X-ray data,ph, and salinity are presented
with the data of other sites in Appendices I, II, III, and IV,
respectively, at the end of the volume.

BIOSTRATIGRAPHY
Foraminifera

Sediments throughout most of the section drilled at Site
219 contain rich populations of planktonic foraminifera
representative of tropical or subtropical environments. The
downhole distribution of planktonic foraminiferal zones isshown on Figure 5. Benthic foraminifera in the recovered
samples suggest as well that during post-Early Eocene time,
water depths at this site have been approximately 2500
meters or greater (lower bathyal or abyssal).
Planktonic faunas indicative of Zone N. 23 (notably,
Globigerinella adamsi) were observed only in the top
sample (Core 1, Section 1, 110-112 cm) but may represent
contamination from unrecovered overlying sediments. The
basal occurrence of Globorotalia truncatulinoides, here
taken as the base of the Pleistocene, is in Core 4, Section 4,70-72 cm.
The Pliocene foraminiferal zones are very poorly
developed. Globorotalia tosaensis is very rare or absent

41

SITE 219
DEPTH

CORE SECT. ZONE

DEPTH

CORE SECT.ZONE

KEY:

well-defined boundary
Doorly-defined boundary
nature and location unknown
unconformity
location of boundary unknown
recovered interval

'N23
N22
5

2

N21
N19-N2O

50
NI 8

NI 7
12

N7-N8

150-1
15

P18

16

6
CC P1745 2 P15

17
18

PI 4
19
20

b
fi
6

PII

CC
P10

?
Mi

Figure 5. Foraminiferal zonation, Site 219, depth in meters.
below the base of the Pleistocene, and the N. 21/N. 20
boundary is placed at Core 5, Section 2, 73-75 cm, thelowest occurrence of G. tosaensis and the highest of
Sphaeroidinellopsis sphaeroides. Zones N. 20 and N. 19
could not be differentiated in this hole.
The basal appearance of Sphaeroidinella dehiscens
immatura, recognized in Core 6, Section 2, 73-75 cm,
marks the base of Zone N. 19, although because thishorizon coincides with the extinction of Globorotalia
margaritae, it appears this event may be somewhat younger
here than elsewhere. The Miocene-Pliocene boundary,defined by the initial appearance of G. tumida tumida, islocated in Core 8, Section 5, 70-72 cm.
Cores 9 through 12 are of Late Miocene (N. 17) age.
Turborotalia acostaensis is common throughout thisinterval; Candeina spp. and Globorotalia tumida plesiotumida are rare but generally present. Significant reworking
from lower Middle Miocene sediments is indicated by thepresence of common Turborotalia siakensis and sporadic
occurrences of Globigerinoides subquadratus and Globorotalia cf. praefohsi.

42

Faunas representative of early Middle Miocene Zone N.
10 are present in Sample 13-1, 68-70 cm. Sample 13-1,
130-132 cm, however, contains a late Early Miocene (N. 8)
fauna, including Globorotalia archeomenardii and Globigerinoides sicanus, indicating a minor unconformity between
these two samples corresponding to a pronounced lithologicchange at this horizon. The remainder of Cores 13 and 14
represent Early Miocene Zones N. 8 and N. 7. Planktonic
foraminifera are particularly abundant in the sediments ofthese cores, which may indicate winnowing of thenannofossils. Alternatively, the generally diminished fragmentation of foraminiferal tests in these samples suggeststhat low levels of calcite solution may have been a factor as
well. It is difficult to visualize changes in productivity
which would increase the foraminiferal populations at theexpense of the nannoplankton, particularly in view of therelatively slow sedimentation rate over this interval.
By contrast, test solution is high in sediments from
Cores 15 and 16, which contain small and relatively
nondiagnostic faunas of Middle to Early Oligocene (P. 18 toP. 19) age. Sample 16, CC and Core 17, Sections 1 through4, contain Late Eocene (P. 17) faunas. Globigerinatheka
semiinvoluta appears in Sample 17-5, 51-53 cm, indicating aP. 15 age assignment and suggesting a minor unconformity(representing Zone P. 16) above this sample. The highest
occurrence of Truncorotaloides pseudodubius, which marks
the top of Middle Eocene Zone P. 14, is present in Sample
18-3, 53-55 cm; faunas of this age persist as low as Sample
19-5, 51-53 cm. Below this horizon is located anotherminor unconformity; in Core 19, Section 6 through Core
20, Section 6, the presence of Morozovella aragonensis
aragonensis indicates assignment to Zone P. 11. Samples 20,
CC through 21, CC are of P. 10 age, based on the presenceof Hantkenina mexicana aragonensis. No foraminifera wererecovered from Cores 22 and 23.
Considerable difficulty was encountered at this andother sites in adequately differentiating early Middle and
Early Eocene zones; this was largely due to the absence ofseveral diagnostic zonal taxa and confusion about theranges of others. As a result, while the samples recoveredfrom Cores 24, 25, and 26 could be recognized as Lower
Eocene (as generally defined by planktonic foraminifera),no definite zonal determinations could be made.
A major faunal discontinuity occurs between Cores 26
and 27. All cores above this horizon contain faunas
composed largely of planktonic species; roughly 90 percentof the specimens in Sample 26, CC are planktonic, although
the ratio is somewhat lower in some Oligocene and Upper
Eocene samples because of selective solution of planktonic
tests. In samples from Core 27 and from most cores in Hole
219A, planktonic foraminifera are relatively rare, andwhere foraminifera are present, benthic species predominate. Core 27 and Core 3A to Core 8A, Section 1
commonly contain significant numbers of benthic andlarger foraminifera, bryozoans, ostracods, and echinoid
spines, a tropical assemblage indicative of inner neritic
water depth. The relative abundance of benthic foraminiferal species decreases somewhat in Cores 5A through 14A,
suggesting slightly deeper (but probably still neritic) water.
In any case, sediments in and below Core 27 were depositedin water much shallower than the sediments above. The

SITE 219

shallow-water sediments are entirely of Late Paleocene (P.
4) age; Globanomalina pseudomenardii is present in
Samples 27-1,100-102 cm and 219A-12-3, 82-84 cm,alongwith other, generally rare, Paleocene species. The
paleoecology of these Paleocene sediments is discussed ingreater detail by the Paleontological Laboratory of theGeological Survey of India (this chapter).

Nannofossils
Hole 219 was drilled in sediments ranging in age from
Pleistocene to Early Eocene. Abundant nannofossils wereencountered throughout most of the section in sediments
deposited in a bathyal environment.
The Late Pleistocene is present in Samples 1-1, 107-108
cm; 1-2, 75-76 cm; and 1-4, 76-77 cm. Gephyrocapsa
oceanica, Gephyrocapsa caribbeanica, Gephyrocapsa protohuxleyi, Helicopontosphaera kamptneri, Emiliania
huxleyi, Cyclococcolithus leptoporus, and Umbilicosphaera
mirabilis are the most common nannofossils noted in Core
1, Section 1 through Core 1, Section 4. The Early
Pleistocene is present in Sample 1, CC and ranges down toCore 4, Section 4, 76-77 cm. The most common
nannofossils of the Early Pleistocene interval are Pseudoemiliania lacunosa, Coccolithus doronicoides, andScyphosphaera campanula.
The Late Pliocene is present in Sample 4-5, 80-81 cm,
and extends down to Sample 6-2, 79-80 cm. Discoasterbrouweri, Discoaster pentaradiatus, and Discoaster surculus
are common nannofossils present in the Late Pliocene
interval. The Plio-Pleistocene boundary is present between
4-4, 76-77 cm and 4-5, 80-81 cm. The interval between 6-3,
79-80 cm and 8-5, 75-76 cm represents the Early Pliocene,and significant nannofossils within this interval include
Sphenolithus abies, Reticulofenestra pseudoumbilica, Discoaster variabilis, Discoaster challengeri, Discoaster asymmetricus, Ceratolithus rugosus, Ceratolithus tricorniculatus,
Discoaster neohamatus, and Umbilicosphaera cricota.
The Miocene-Pliocene boundary, as defined by nannofossils, occurs between 8-5, 75-76 cm and 8-6, 75-76 cm
and is based on the extinction level of Discoaster
quinqueramus in 8-6, 75-76 cm. Discoaster calcaris,
Discoaster quinqueramus, and Triquetrorhabdulus rugosus
are commonly present in the Late Miocene interval. The
middle Miocene-Late Miocene boundary occurs between
9-4, 75-76 cm and 9-5, 75-76 cm and is based on theextinction level of Discoaster hamatus. The Middle Miocene
interval ranges from 9-5, 75-76 cm down through 13, CC.
Middle Miocene nannofossils present within this interval are
Discoaster hamatus, Scyphosphaera amphora, Catinastercoalitus, Discoaster dilatus, Discoaster perclarus, Coccolithus neogammation, Discoaster kugleri, Discoaster exilis,
Sphenolithus moriformis, and Sphenolithus heteromorphus.
The Early Miocene ranges from 14-1, 79-80 cm to 14, CC,
and nannofossils common to this interval are Discoastermolengraafi, Coccolithus aff. C. bisectus, Sphenolithus
belemnos, Sphenolithus conicus, Helicopontosphaera
ampliaperta and Discoaster nephados. The early Early
Miocene and Late Oligocene were not cored in this hole.

The Middle Oligocene ranges from 15-1, 79-80 cm to 15,
CC. Coccolithus eopelagicus, Coccolithus bisectus, Sphenolithus distentus, Sphenolithus predistentus, Helicopontosphaera compacta, Discoaster woodringi, and Discoasterdeflandrei are present in the Middle Oligocene interval. The
Early Oligocene ranges from 16-1, 78-79 cm to 16, CC andcommon nannofossils present in this interval include
Braarudosphaera rosa, Micrantholithus flos, Reticulofenestra umbilica, Cyclococcolithus lusitanicus, Discoastertani tani, Discoaster plebeius, Discoaster germanicus, andIsmolithus cf. recurvus.
The Eocene ranges from 17-1, 127-128 cm down to
27-1, 123-124 cm. The Oligocene-Eocene boundary ispresent between 16, CC and 17-1, 127-128 cm, and Late
Eocene sediments are present down to 18-3, 79-80 cm.
Cyclococcolithus formosus, Discoaster saipanensis, Discoaster barbadiensis, and Syracosphaera bisecta are commonly seen in the Late Eocene interval. The Middle Eocene
interval extends from 18-4, 82-83 cm to 24, CC. Common
Middle Eocene nannofossils seen in this hole include
Chiasmolithus grandis, Sphenolithus obtusus, Sphenolithus
spiniger, Sphenolithus radians, and Discoaster sublodoensis.
The Early Eocene is present in Core 25, and Discoasterlodoensis is present within this interval. Nannofossils are
not present in 27-2, 75-76 cm and 27, CC. The sediment in
the bottom of Core 27 is largely composed of recrystallized
calcite laths. A bit sample from Core 28 reveals a total
absence of nannofossils.
Hole 219A was drilled in sediments of Paleocene age.
Environments encountered throughout the cored section
indicate marine continental shelf-type deposition withconditions favorable for the formation of glauconite.
Nannofossils are rare and corroded in Cores 4, 5, 6, 7, 8, 9,
10, 12, and ,14. The presence of Cruciplacolithus tenuis in
10-3, 124-125 cm was established. Poor preservation of
nannofossils in this interval is detrimental to proper
identification of individual species and an accurate age
determination was not obtained in the bottom of this holefrom nannofossil data.
Radiolaria

Rare, often fragmented, specimens of Radiolaria arepresent in the core catcher samples of Cores 1 through 10.
No age assignment based on Radiolaria was possible in thisinterval. Radiolaria are absent from Core 11 throughSample 16-5, 12-14 cm. At 16-5, 28-30 cm, a richradiolarian fauna appears that belongs to the Thyrsocyrtis
bromia Zone, which spans the Eocene-Oligocene boundary.
There is no obvious megascopic change in Lithology
between the radiolarian and nonradiolarian parts of thecore. The base of the T. bromia Zone lies between Core 18,
Sections 4 and 5.
Between Core 18, Section 5 and Core 19, Section 5 theradiolarian fauna is characteristic of the Podocyrtis mitra
Zone (Middle Eocene). Both Podocyrtis chalara andPodocyrtis goetheana are absent from Site 219 and so it is
not possible to recognize the P. chalara and P. goetheana
zones, as described by Riedel and Sanfilippo (1970) and by
Moore (1971).
Below the P. mitra Zone lies a new zone, the Podocyrtis
ampla fasciolata Zone (Middle Eocene) which seems to43

SITE 219

parallel stratigraphically the Podocyrtis ampla ampla Zoneof Riedel and Sanfilippo (1970). P. ampla ampla is absent
from the present material. For discussion of this new zone
see Nigrini (this volume*). Between the P. mitra and P.
ampla fasciolata zones there is an apparent faunal gap
owing to the formation of chert in Core 19, Section 6.
Radiolaria are common and well-preserved in Core 19,
Section 5 and Core 19, CC, but are almost absent fromCore 19, Section 6.
The Thyrsocyrtis triacantha Zone (Middle Eocene)
extends from Core 20, Section 6 to Core 21, CC. Core 21
bottomed in chert.
Below the chert layer, in the core catcher sample of Core24, a sparse and poorly preserved assemblage appears tobelong to the Theocampe mongolfieri Zone (lower Middle
Eocene). Radiolaria were not found in subsequent Site 219
cores.
Benthonic Foraminifera2

A total of 33 samples has been studied out of which four
samples, i.e., 219A-13-2, 60-63 cm; 219A-11-2, 82-83 cm;
219A-10-3, 130-131 cm; and 219A-10-2, 127-128 cm fromthe Lower Paleocene are devoid of any benthonicforaminifera. However, the overlying and underlying
samples have yielded a fairly continuous assemblage.
Absence of benthonics in these samples may be ascribed to
local unfavorable ecological factors.
Sixty-six genera have been identified, the majority ofthem ranging from Cretaceous to Recent with wide
geographical distribution.
The larger foraminifera are represented by Discocyclina
ramaraoi Samanta, Discocyclina sp., Operculina canalifera,
and Operculina sp.
It may be noted that Cibicidina sp. has been reported
only from Eocene strata in North American (Loeblich andTappan, 1964, p. 686), but in the present assemblage
Cibicidina sp. has been found dating back even to Early
Paleocene.
The fauna is predominantly calcareous, only seven
genera of arenaceous foraminifera, representing 10 percentof the total fauna, are present, suggesting an open-sea
depositional environment.
The total benthonic foraminiferal percentage by dry
weight is less than one percent in Lower Paleocene
sediments, but it rises to three percent in the Middle
Paleocene and then again declines in the Upper Paleocene.
It suddenly jumps to 12 percent towards the top of the
Paleocene and declines again towards the Lower Eocene,reaching less than one percent from the top of the Lower
Eocene to the Lower Oligocene.
The distribution of benthonic foraminiferal genera indifferent samples and their state of preservation with
foraminiferal percentage curve are depicted in Table 3.
The benthonic foraminiferal assemblage is similar to the
Indo-Pacific foraminiferal fauna recorded from the east
coast of India and from the Saipan Islands.
The characteristic foraminiferal species Discocyclina
ramaraoi Samanta (Samanta, 1967), with variation from2
V. D. Mamgain, B. P. Chatterjee, M. K. Sen, and R. S. Misraof the Paleontology Division, Geological Survey of India under theguidance of M.V.A. Sastry.
*"This chapter will now be published in Volume 24 of theInitial Reports series."

44

flat to triagonal shape of its test, is represented in thepresent assemblage. This species is known from thePondicherry Formation (Middle Paleocene to basal Eocene)of the east coast of India and has not been recorded, so far,from any other localities in India. Its presence, therefore,suggests the possibilities of intermingling of the fauna of
the east coast of India with the fauna from this site.
The general pattern of the benthonic foraminiferal
assemblage and the abundance of larger foraminiferal
genera towards the close of the Paleocene suggests an
open-sea shallow-water neritic environment of less than 100
meter water depth for Site 219 during most of Paleocene
and Eocene times.
Ostracods3

A study of the ostracod fauna was made from the same
samples as those examined for benthonic foraminifera. Outof the 33 samples studied for foraminifera between the
Samples 219-15-1, 100-102 cm to 219A-14-3, 138-140 cm
only 14 samples yielded ostracods. The amount of ostracod
fauna by dry weight percentage is negligible, and they arepresent in traces only. Their state of preservation is poor
between Samples 219A-14-3, 138-140 cm and 219A-4-3,
60-62 cm. The rest show fair to good preservation.
Sixteen genera belonging to nine families are present in
the assemblage with the genera Bairdia, Cytherella, Krithe,and Loxoconcha being the most common. The presence ofCytherelloidea in Samples 219-14-3, 138-140 cm and219A-7-3, 48-49 cm suggest shallow, warm sea conditions.
The interval between 219A-3-2, 119-120 cm, to 219-27-1,
60-61 cm suggests an epineritic environment of deposition
with maximum development of ostracod fauna. From
Sample 219-25-1, 138-140 cm and above, deep water genera
such as Paracypris, Bythocypris, and Macrocypris are alsopresent in the assemblage suggesting a gradual deepening of
the site.
The general faunal pattern supports the evidence frombenthonic foraminifera of a shallow epineritic to neritic
environment throughout the Paleocene and up to the basal
Eocene with a gradual deepening during the latter part of
Early Eocene and later times. The distribution of the genera
is shown in Table 4.
Biostratigraphic Summary

Nannofossils and planktonic foraminifera are common
to abundant throughout most of the sediments collected inHole 219, although both become rare to absent in Hole
219A. Faunal assemblages in this latter interval aredominated by such benthonic fossils as benthic and larger
foraminifera, bryozoans, and ostracods. Radiolaria are rareor absent in post-Eocene sediments, well-developed in theUpper and Middle Eocene, again rare to absent inpost-Eocene sediments, well-developed in the Upper andMiddle Eocene, and again rare to absent at lower horizons.
Pleistocene sediments are present as low as Core 4,
Section 4 (0 to 30 m), and contain abundant andwell-developed nannofossil and foraminiferal assemblages.
The Miocene/Pliocene boundary, as recognized here (top of
Discoaster quinqueramus Zone), occurs in Core 8, Section 6(69 m). The interval between Core 8, Section 6 and Core 9,
J

Paleontological Laboratories of the Geological Survey of India.

SITE 219
Section 4 contains sediments of Late Miocene (N. 17, D.
quinqueramus Zone) age.
The interpretations of the sediment ages from Core 9,
Section 5 through Core 12, CC are at variance, and it has
not been possible to reconcile them. Nannofossil floras
indicate a Middle Miocene,/), hamatus Zone, age, while theplanktonic foraminifera suggest that this interval should be
assigned to Zone N. 17, with considerable Middle Miocene
reworking. The reader is advised to examine the nannofossil
and foraminifera reports in this chapter, as well as the
special chapters involving these groups (Boüdreaux, Bukry,
Fleisher*, and Akers*, all this volume).
Middle and Lower Miocene sediments were recoveredfrom Cores 13 and 14 (119 to 137 m), although there issome disagreement between nannofossil and foraminiferal
determinations as to where the boundary between themshould be placed. Planktonic foraminifera are particularly
abundant in samples from these cores, which may be theresult of winnowing of the nannofossils or, in part, ofdecreased solution of foraminiferal tests.
Middle and Lower Oligocene sediments are present inCores 15 and 16 (156 to 174 m). Radiolarians become
abundant in Core 16, Section 5 (173 m), although they areabsent in overlying strata. Late Eocene assemblages wererecovered between Sample 16, CC and Core 18, Section 2(174-186 m); this interval appears to contain a minor
unconformity at 180 meters. A second Eocene unconformity at 200 meters is present within the Middle Eocene
sequence.
Fossil assemblages recovered from Cores 24 through 26(237-264 m), below the chert, contain common foraminifera, while radiolarians and nannofossils are rare toabsent. These assemblages represent Lower Eocene deep-sea
sediments. Core 27, however, is dominated by shallowwater (neritic) benthonic organisms; the rare planktonic
foraminifera in this core and in samples from Hole 219A
indicate that the shallow-water sediments in which this site
was drilled (264 to 411 m) are entirely of Late Paleocene(foraminiferal Zone P. 4) age.
Sedimentation Rates
The fluctuations in the sedimentation rate at Site 219
probably reflect the fact that the site lies on the crest of aridge. Shallow-water sediments of Paleocene age (264 to
405 m) accumulated at a rate of at least 70. m/m.y. (seeFigure 6). In portions of this sequence, the sediments
consist largely of the fossils of benthonic organisms. Lower
and Middle Eocene sediments of deep-sea origin, separated
from the Paleocene sediments by a significant unconformity (at approximately 260 m), accumulated less rapidly(18 m/m.y.).
A second unconformity at 200 meters is overlain by acontinuous sequence of Middle and Upper Eocene
sediments; the sedimentation rate of these deposits is notclearly established, but was at least 9 m/m.y. The Late
Eocene to Middle Oligocene sequence (156-177 m) above
the third unconformity (between Sections 4 and 5, Core17, at approximately 178 m) was deposited at the lowest
sedimentation rate observed at this site (2 to 5 m/m.y.).
Above this interval, Lower Miocene sediments were
deposited somewhat more rapidly (5 to 11 m/m.y.);whether an unconformity separates the Miocene and*"This chapter will now be published in Volume 24 of theInitial Reports series."

Oligocene cannot be determined due to nonrecovery(drilling) of the appropriate horizons. Another unconformity between Middle and Lower Miocene deposits
within Core 13 (at 121 m) probably represents no morethan 1 m.y.
The age of sediments between 77 and 100 meter has notbeen clearly established; alternative interpretations areshown on the accompanying chart. Minimal rates of 12 and31 m/m.y. have been calculated for this interval, on thebasis of nannofossil and foraminiferal determinations,
respectively, but paleoπtological control is inadequate for amore precise calculation. The nannofossil ages for thesesediments indicate the* presence of an unconformity (at76 m) above this interval; if the foraminiferal ages arecorrect, one may instead be present within the drilledinterval separating Cores 12 and 13. The Upper Miocene toPleistocene sediments (0 to 64 m) accumulated at the rateof 14 m/m.y.
GEOCHEMISTRY

The nanno ooze recovered from the upper 100 meters at
Site 219 is apparently enriched in magnesium, titanium,
chromium, copper, nickel, iron, and vanadium, comparedto the sediments recovered from the basal 130 meters(Figure 7).
There is also a high correlation between concentrationsof titanium, copper, chromium, nickel, iron, and vanadium.
This suggests that these elements are contributed by a single
mechanism, and that they have suffered little postdepositional migration. A preliminary examination of smear
slides of sediments from Site 219 shows the presence of
detrital material only in these upper 100 meters of
sediments.
It is conceivable that during deposition of the upper 100
meters of the section, Site 219 was in a position to receive
more detrital material than during the interval from 100 to
230 meters.
Another interesting feature of the section examined is anapparent correlation between the barium concentration andthe relative abundance of nannofossils in the sediments
as determined by smear slide examination. This associationof barium with the biogenic aspects of oceanic sediments
has been noted by various authors. Goldberg and Arrhenius(1958) have shown that in the areas of high productivity inthe equatorial Pacific, the barium concentrations of thesediments are high. Turekian and Tausch (1964) also noted
a similar relationship of barium to high productivity in thesediments of the Atlantic Ocean. Thus, the distribution of
barium in the sediments of Site 219 could be related to
productivity.
MINERALOGY AND K-Ar DATINGOF GLAUCONITE4At Holes 219 and 219A, 265 meters of Recent toEocene deep-water pelagic oozes and chalks, containing
mostly nannofossils and planktonic foraminifera, were
found to overlie shallow-water sediments. The latter consist of chalks and limestones (60 m) with larger foraminifera.
They are underlain by 90 meters of glauconitic limestones
and glauconitic siltstones (see Lithology Section).
J. Hunziker and A. Matter.
45

SITE 219

1

Good
Good

c

Fair
Bad
Poor
Fair
Fail

Poor
Bad
Bad
Bad
Bad

c.
<;

X

Bolivinitidae

X

Turrilina

Buliminella

Tristix

Bolivina

X

TurrUinidae
OolinaX

Fissurina

X

Polymorphinidae
X

Glandulinidae

Saracenaria
X

X

Glandulina

Pseudonodosaria
X

X

Vaginulina

Nodosaria
X

X

Polymorphina

Lenticulina

Nodosariidae
Triloculina

Fischerinidae

Miliolidae
Quinqueloculina

Verneuilina

Fischerina

4 taxophragmiidae
Tritaxia

Vulvulina

Gaudryina

Textulariidae
Textularia?Haplophragmoides

Semivulvulina

X

X

X
X

X

X

X

X

X

X

X
X

X
X
X

X
X

X

X
X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X
X

X

X

25, CC
26-1, 17-19

X

26-1,135-137

X

X

X

X

X

X
X

X

X

X

27-1,95-96

X

X

X

X

X

X

X

X

X

X

27-1, 148-150
27-3, 90-92

X

219A-3-1, 139-140

X

3-2, 27-28
3-2, 119-120

X

X

X

X

X

X

X

X

X

X

X

X

X

X

4-2, 124-125

X

X

X

X

X

X

X

5-2, 117-120

X

6-2, 34-35

X

X
X

X

X
X

8-3,56-57

XX

X

8-5,22-23XX

X

10-2, 127-128
10-3, 130-131

al 1-2, 82-83

12-3, 115-116
a

X

X
X
X
X
X

X

X

X

X

X

X
X

X

X

X

X

X

X

X
X

X
X

X

X

7-3, 48-49

a

X

X

8-2, 35-40
X

X

X

X

4-3, 60-62

a

X

X

X

27-1, 60-61

X

X

X

X

X

X

X

X

X

X

X

X

X

l 3-2, 60-63

14-3, 32-33

Poor

14-3, 138-140jX

21-2, 120-122

Bad

No benthonic foraminifera.

46

X

J

20-2, 120-122

25-1, 138-140

1

Fair

a

19-6, 100-102

X

Early

Bad

X

1
1

Paleocene

Fair

18-4, 40-42

Early

Fair
Good
Fair

X

25-1, 108-110

Good
Good

16-6, 70-72

Late

Good

219-15-5, 100-102

EoceneFair

Dentalina
Lagena

Fair

Fair

X

Early

'

Good
Good

X

1

C%

5%

Middle Late'

Percentage Curve

Benthonic
10%

Middle1
Good

Sample(Interval incm)

HorizonOligocene

15%

Foraminiferal

State ofPresservation

Lituolidae

TABLE 3Distribution of Benthonic Foraminiferal Genera, Site 219

X

X
X

X

X

X

X

X

X

X

Uvigerinidae
Discorbidae

Discorbis

X
X

X

X
X

X
X

X

X

X
X

X

X
X
X

X

X

X
X

X

X

X

X

X

X

X

X

X

X

X

X
X

X
X

X
X

X

X

X

X

Spirillinidae

Nuttalides
Conicospirillina

X

X
X

X
X

X
X

X

X

X
X

X

X

X
X

X

X

X

X

X

X
X

X

X

X

X

X

X

X

X
X

X

X
X

X

X

X

X

X

X
X

X

X
X

X
X

X
X

X
X

X
X

X
X

X

X

X

X

X

X

X

X
X
X
X
X
X

X
X
X
X
X
X

X
X
X
X

X
X
X

X
X
X
X

X

X
X

X

X

X
X

X
X

X
X
X

X
X
X

X
X
X
X

X
X
X
X
X

X
X

X
X
X

X

X

X

X
X

X
X

X
X

X
X

X

X

X

X

X

X

X

X

X

X

Nonionidae

X
X
X

X
X
X
X

X
X

X
X

X

X

X

X

X

X

X

X

X
X

X
X

X
X
X

X
X
X

X
X

X

X
X

X

X

X

X
X

X

X

X

X

X

X
X

X
X

X

X

X
X

X
X

X
X

X
X

X

X

X

X

X
X

X

X

X

X

X

X

X
X

X
X

X

X
X

X

X
X

X
X
X
X

X
X
X
X

X
X
X

X

X

X

X

X

X

X

X

X
X

X

X

X
X

X
X

X
X

X
X

X
X

X
X

Lamarackina

Hoeglundina

Epistomina

Heterolepa
Ceratobulimindae

Anomalinidae

Osangularia
Anomalina

X

Gavelinella

Osangulariidae

Svratkina

Gyroidina

Alabamina

Pullenia

Nonionella
Alabaminidae

Loxostomidae

Loxostomum
Astrononion
NonionX

Florilus

Pleurostomellidae
Caucasinidae?Caucasina

Discocyclinidae

Cibicididae

Eponididae

Pleurostomella

Discocyclina Sp

Discocyclina Ramaraoi

Planulina

Gbicidina

Cibicidella

Cibicides

EponidesCibicorbis

Operculina Sp B

Rotaliidae
Nummulitidae

Rotalia
Operculina Sp A

Spirillina

Patellina

Siphonninidae
Epistomariidae

Siphoninella

Valvulineria

Epistominella

Buliminidae

Reusella
Uvigerina

Eouvigerinidae

Bulimina?Eouvigerina
Stüostomella

SITE 219

TABLE 3 - Continued

X

X

X

X
X
X

X

X

X

X

X
X

X

X
X

X

X

X

X

47

SITE 219
TABLE 4
Distribution of Ostracod Fauna, Site 219

MiddlePaleocene

Late

Early

EoceneMiddle Late

Oligocene219-15-5,100-102
219-16-6,70-72
219-18-4, 40-42
219-19-6,100-102
219-20-2,120-122
219-21-2, 120-122
219-25-1, 108-110
219-25-1, 138-140
219-26-1,17-19
219-27-1, 60-61
219-27-1,95-96
219-27-1,148-150
219-27-3, 90-92
219A-3-1, 139-140
219A-3-2, 27-28
219A-3-2, 119-120

X

X

Hermanites
Occultocythereis
Quadracythere
Trachyleberidea
Cytherella
Cytherelloidea

X

Loxoconcha
Schizocythere
Trachyleberis

Paraypris
Brachycythere?Alatacy there
KritheSample(Interval in cm)

HorizonBairdia
Bythocypris
Macrocypris

Genera

X

X

X

X
X

X

X

X
X

X

X
X

X

X

X

X

X

X
X

X

X

X

X

X

X

X

X

X

X

X

X

X
X

X

X

X

X

X

X

219A-4-2, 124-125
219A-4-3, 60-62

X

219A-5-2, 117-120
219A-7-3, 48-49

X

X

X

X

X

X

X

X

X

X

X

X

X

X

Early

219A-8-3
219A-8-5, 22-23
219A-14-3, 32-33
219A-14-3, 138-140

In contrast to the pelagic section where paleontologic
control was excellent, only a general Paleocene age could be
assigned to the shallow-water sediments because of theirpoorly developed microfossil assemblages. Therefore, it was
decided to attempt glauconite dating with the potassiumargon method.
Two samples were studied, one, 219A-9-5, 5-40 cm,
where paleontologic control was still available (Paleocene)
and the other, 219A-14-4, 0-25 cm, from the bottom of theborehole and of unknown age.
Under the petrological microscope, the upper sample is asandy, zeolite- and glauconite-rich biomicrite. Light to darkgreen "glauconite" occupies the cells and chambers ofbryozoans, echinoderms, coralline algae, and larger

48

X
X

X

X

X
X

X

X

X

X

X

X

X

foraminifera and replaces parts of pelecypod shells and,especially, the glassy matrix of sand- to silt-sized volcanic
rock particles. The lower sample, though similar, is finer
grained, much more recrystallized, and contains less"glauconite" (<15%). There the "glauconite" is a brownish
green color.
The samples were first disaggregated using 5 percent
acetic acid to get rid of the carbonate and then sieved andpassed through a magnetic separator.
The fraction 0.175 to 0.150 mm was crushed and
X-rayed after various treatments to identify the nature ofthe "glauconite." The green mineral from Core 9 is
identical to what Porrenga (1967) named "proto"
glauconite (see loc. cit, fig. 38) and which is actually

SITE 219

()

10
20
PTPUO
MIOCENEo |E |LATE|MID.|EARLY

1

TABLE 5
Radiogenic Ages of Site 219 Samples

30
40
50
60
M.Y.
OLIGOCENE
EOCENE
PALEOCENE
AGE
LATE | M.| E. LATE|MIDDLE| E. LATE | E.

219A-9-5,
05-40 cm

3.89

Rad
(%)
56.2

219A-14-4,
0-25 cm

4.31

56.1

^-2

A4-1
\4-5
^A-6-3
•A 8-1
V8-6
100-

Jl2-6µ-\l2-6• • •••• • •• •••• • j K ^ • ^ g•

DEPTH IN HOLE (METERS)(5^1V) V.14-6

-17-1

ro
o
o

3

^9) V "
T i 9-6
r20-cc@V24-i27-1'µ3004A-4(>7θ)• 12A-3400-

2.4343.9 ±3.1

PHYSICAL PROPERTIES
Sediment Density, Porosity, and Water Content

Wδ-i
A-26-1Age(m.y.)
41.6 ±3.0

Both ages are Eocene and not Paleocene as shown by the
paleontological evidence. Statistically, the two ages are notsignificantly different.
The X-ray analysis shows that the green mineral is not aglauconite sensu stricto. Obradovitch (1965) and Odin (inpress) have already cautioned against using glauconites ofthis type for age determinations because readings may be
up to 30 percent too low. Apparently, the lattice ofmontmorillonitic glauconites is not a closed system. The
erroneous ages are, therefore, either due to argon loss or
absorption of potassium or both.

F

18

K
(%)
2.32

14A-2

Figure 6. Sedimentation rate curve, Site 219. Plotted bars
are those sufficient to control slopes of lines. Stippled
pattern represents some uncored intervals. See Chapter
2, Explanatory Notes, for explanation of age ranges andother symbols.
montmorillonite. The brownish-green "glauconite" fromthe bottom of the borehole is also a montmorillonite
mineral but probably a nontronite-like variety. This issuggested by its behavior after heating to 55O°C, where allreflections disappear. A similar montmorillonite was notedin the Red Sea. A more detailed account of the nature andmineralogy of the "glauconites" from Site 219 will be
published later.
Potassium was determined by flame photometry. Argon
was extracted from the minerals with a high frequency
furnace and measured by isotopic dilution using an A r 3 8
spike.
Isotope ratios were obtained on a GD 150, 180°mass
spectrometer of Varian MAT Bremen (Germany), which isoperated statistically. On the basis of interlaboratory
standards, the accuracy of this technique for K plus Ar is
estimated to be ± 4 percent, line and techniques have been
described by Purdy (1972).
The samples yielded the ages given in the following
table, (Table 5).

No major variation in density is evident over the upper
100 meters at this site. The first 12 cores recovered
display a steady, but slight, gradient from 1.56 to 1.70 g/cc,
presumably related to increasing sediment compaction. This
interval corresponds to lithological unit I which shows only
gradual lithological variations with depth. Water content
varies little from a mean at about 37 percent.
A general drop in density occurs in Cores 13 and 14
together with water content values which increased toaround 47 percent. These features can be related to the unit
II lithology of foram ooze and chalk since the hollow foram
tests would be expected to cause such effects.
Between 150 and 220 meters, over the interval of Cores
15 to 21, a greater fluctuation in density is evident. Water
content also fluctuates between 28 and 42 percent. The
GRAPE density plots on the core summary logs show aseries of rapid changes. The unit HI lithology, analternation of oozes with harder chalk layers, accounts forthese fluctuations.
Plotted data are sparse below this level, but Core 26
displays a major density increase to 2.0 g/cc, and in Hole
219A, downward from 300 meters, density fluctuatesmarkedly around a mean of about 1.8 g/cc.
Compressional Wave Velocity

Over the upper 100 meters, velocity can be expected,
due to the homogeneous nature of the lithology, to remain
at around 1.54 km/sec as measured in Core 4.
A slight rise is evident in unit II (foram ooze and chalk)with values of up to 1.70 km/sec for the chalks in Core 14.
Chalks in unit III (alternating ooze and chalk) have valuesof up to 1.84 km/sec.
A major peak in the velocity plot occurs at the base ofCore 21, where values reach 4.0 km/sec. This reflects achert layer, and other such layers in the interval of unit IV
give values approaching this, as peaks above a general levelof about 2.0 km/sec.
Below 326 meters, marked fluctuations in velocity aredisplayed, rising to just over 4.1 km/sec. These appear to49

SITE 219
Meters Barrel Lithology'
π
u
1
_-Λ

2 23

_L

4

- I "_L
_L
_L

5
50

Mg

Ti

Mn

Cr

Cu

Ni

Fe

••••••

••i^•

•^

•••
•••

•

1

"""
••-•

" ^
•••

"™

1

^•

I"]

V

SITE 219
Ba

••

•••-j

6 ^"7
8
9 -L.
10 - 1 11

100

F
_L

•

_1_ F_

_L

^•

••••

•

•••••

•••••

1

I

1

•

••

•

1

••i

•

--

Z

M••

1

"F
4J

12

^ ^ • l

^™

••

••
••

™

••
••
"

••^

•

•

1

•

•

1

1

•

•

1

•

——i

i

I

•

•i

-

-l_
T
-L-

13

T

-–

"Wfir

14 -i- -1~i'-115 _i_

16

J. T
J. T
_l_

17 - . n
18
200

"*" ^

_L

19 _L
20
21

i

r1

150-

••i

α α
3 O

c F

fσ c

.-\

•••
•••

•1

•

—
.
1

•
•

•

•
•
•
•

•
1

•••

1

•

•••

1

1

•

•

•
•

•
H i

••

i

•

n•

•H•

22
0.0 0.5 1.0 0.0 0.10.2
Wt. %
wt. %

O~ iölOOO 0 ~ O~TOO
wt. %
ppm

0

10 20

ppm

O~

ppm

Wt. %

ppm

ppm

Figure 7. Chemistry of the sediments from Site 219.
correlate with glauconite-rich limestones and glauconitebearing siltstones. A value of over 5.3 km/sec was recorded
from a limestone in 219A-10-2.
Specific Acoustic ImpedanceThis parameter bears an inherent relationship to thereflection coefficient and so should identify the majorreflectors. Its plot almost parallels the sonic velocity graphand thus shows the major physical boundaries to be at
depths of 219 and 308 meters.
When a comparison is made with Francis and Shor's(1966) nearby seismic refraction station at 9°N, their belief
that the upper refracting horizon, with a measured velocityof 3.85 km/sec, was volcanic rock appears unfounded sincevelocities approaching this value are shown to be present in
the glauconite calcareous sandstone sequence and reach 4.0
km/sec in the cherts and limestones above this.
CORRELATION OF REFLECTION PROFILES
AND LITHOLOGIES

Two reflectors can be consistently identified in theregion around Site 219 (Figure 8). The upper reflector isweak and lies in the lower half of an acousticallytransparent layer. At the base of this layer, a strong but
diffuse reflector, typically spread over 0.3 seconds, is50

ubiquitous. A careful study of this reflector reveals that itprobably consists of two sets of merged reflections. Rare
hyperbolic echoes near the base of the diffuse reflector
suggest the presence of an irregular, even deeper, surface.
The observed reflections at this site occurred at 0.17,
0.28, 0.42, and at about 0.55 (hyperbolic echo) seconds of
two-way travel time below the sea bed. These times areindicated on Figure 9. Also indicated on this figure are thedepths of various lithologies which showed an appreciable
increase in hardness compared with the immediately
overlying rocks.
The first such lithology is the foram chalk, first cored inCore 13 (119-128 m). It occurs as hard bands between bedsof ooze, and after Core 13, circulation was required to cut
the cores. The chalk undoubtedly gives rise to the weak
upper reflector in the transparent layer. This is alsosuggested by the greater density of the chalk, compared tothat of the ooze.
The next deepest reflection, which appears on therecords as the top of the strong diffuse reflector, wasdiscovered to be due to Early and Middle Eocene chert
stringers. The first chert was encountered in Core 19 at 200
meters; other cherts occurred sporadically in the underlying
57 meters. The chert has a density of 2.0 g/cc and avelocity of 4.0 km/sec and hence provides a high acoustic
contrast with the overlying chalk and ooze.

SITE 219
Glomar Challenger 23
1923 hrs.

March 13, 1972

1946 hrs.
1
SOUTH

NORTH

-2.0

UPPER
REFLECTOR QO'DIFFUSE REFLECTOR

-3.0

B

A
KILOMETERS

Figure 8. (a). Seismic reflection record obtained on departure from the site along a north-south track. The ship passed within
200 meters of the beacon. The vertical line represents the approximate extent of penetration of the drill string. (b).A line
drawing showing the interpretation of Figure 8 a used to construct Figure 9. The vertical line has tenth second divisions.
No core was recovered between 273 and 299 meters.
Above and below this gap, the main lithologies are chalkand limestone, respectively. Consequently, the 0.42-sec
reflector may be assigned to the boundary separating theabove contrasting lithologies, but in view of the unrealistic
interval velocity which results, the reflector is correlatedwith the top of the sandstone at 327 meters.
From the above conclusions regarding the correlation ofreflections with lithological boundaries, it is only possible
to precisely calculate the mean velocity to the chert, whichis 1.54 km/sec. If the rare hyperbolic echoes represent true
igneous basement, then this lies at a depth of at least 425
meters.
PALEOMAGNETIC MEASUREMENTS

All 11 samples taken for preliminary paleomagnetic
study at this site were from lithological unit V. The
sampled interval covers a time span of about 4.5 m.y.
within the Paleocene sequence.
An essential magnetic characteristic of these samples,apart from Samples 219A-7-3, 77 cm and 10-1, 99 cm, isthe low intensity of the natural remanent magnetism(NRM) (mean value 2.1 ± 0.5 X I0"7 G/cm 3 ). All measurements were completed using a long-spin time constant (528revolutions) in order that an improved signal to noise ratio
could be achieved. However, despite this precaution the
scatter of repeated measurements remained high and thereliability of the results, presented in Table 6, isquestionable.
On the basis of repeat measurements after 6 months
storage and partial alternating field (Af) demagnetization ata peak field of 50 oersteds, it is evident that, on the whole,
the group of samples has low stability. Two samples,
219A-7-3, 77 cm and 14-2, 118 cm, were subjected toprogressive partial Af demagnetization to peak fields of 200
oersted. The results of this procedure are presented in Table
7. Figure 10 shows the plot of relative intensity (J/J o )against demagnetization field for both samples. Sample
219A-14-2, 118 cm shows some indication of stability inthat 50 percent of the original NRM remains after
demagnetization in peak fields in excess of 100 oersted.
The increase in intensity observed on demagnetization at apeak field of 200 oersted is thought to be an instrumental
effect. While it is difficult to be certain from the migration
pattern of the remanent vector during demagnetization as

51

SITE 219

samples, such as 219A-10-1, 99 cm, 14-2, 118 cm, andpossibly, 219A-14-4, 54 cm, which appear to have betterstability, have significantly higher inclination values in therange 35° to 50° (after demagnetization) and thus indicate
paleolatitudes within the range 20 to 30°S. Such a range isin broad agreement with the expected position of the Indian
plate based on the reconstructions of McKenzie and Sclater(1971).

DEPTH, METERS
200

300

0.1-

DISCUSSION AND CONCLUSIONS

0.2-

Subsidence of the Site
0.3-

0.4-

0.5-

Figure 9. Plot of reflection times beneath Site 219 against
the depths of significant changes in lithology found in
the cores. Lines are drawn corresponding to mean
velocities of 1.5, 1.6, 1. 7, and 1.8 km/sec.
to the stable direction of any underlying hard magnetization component, there is some suggestion that this may
be associated with an inclination around 50°.
The mean inclination calculated for all samples after
demagnetization is 29.1 ±5.6 degrees. Such an inclination
would correspond, accepting an axial dipole approximation,
to a paleolatitude for the site in Paleocene times of 15.5°S.
This result appears to be widely discrepant from that of
40° S given from the Deccan Trap data by McElhinny(1968). The presence of appreciable viscous magnetization
components may account to some extent for the
anomalously low value of absolute inclination that isobserved when the samples are considered as a group. Those

The Paleocene sediments exhibit conclusive evidence
that they were deposited in shallow water. On the evidenceof the benthonic foraminifera and the abundance of larger
foraminifera, the depth is estimated to have been about 100
meters. Additional indicators of shallow water are
glauconite, cross laminations, fragments of pelecypods,coarsely ornamented ostracods, red algae, bryozoans, andechinoids. At present, the site lies in 1764 meters of water.
Since the depth of deposition of the oldest sediments
recovered from this site was 100 meters, and because thesesediments are now found 411 meters below the sea floor,
the sea floor at this site has sunk 2075 meters since early
Late Paleocene time (ca. 58 m.y. ago), indicating a mean
subsidence rate of 36 m/m.y. Sinking had probably begun
by Late Paleocene time simply because there are at least
150 meters of shallow-water sediments, but the
sedimentation rate of at least 70 m/m.y. was clearlyadequate to approximately keep pace with the sinking.
However, around the Paleocene/Eocene boundary there
appears to have been a period of nondeposition lasting
about 5 m.y.; after this, the sedimentation rate was only 18
m/m.y. In addition, the Lower Eocene benthic foraminifera
indicate a bathyal environment. This indication of a
relatively sudden increase in water depth can probably be
explained by a combination of nondeposition for about 5
m.y. and continuing steady sinking at around 70 m/m.y.
The sinking history of the site since the Early Eocene is notknown except that it probably did not exceed the rate
which allows coral growth upwards to keep pace withsinking since the coral atoll of Minikoi lies 45 miles to thesouth. In fact, figures quoted by Seibold (1972) indicatethat vertical reef growth can reach 20mm/yr. This rate isunlikely to have been exceeded by the sinking. Pacific atolls

TABLE 6
Summary of Magnetic Data, Hole 219A
NRM

52

Sample(Interval in cm)

Intensity(G/cm3)4-2, 56
4-2, 34
4-4, 101
6-1,71
6-2, 68
7-3, 77
9-5,47
10-1, 99
10-2, 129
14-2, 118
14-4, 55

1.3 x 10-7
1.2 x I0"7
3.8 x 10-8
2.0 x I0"7
1.8 x I0"7
2.1 x 10-6
1.3 x I0"7
4.5 x I0- 7
4.3 x I0"7
1.1 x 10-5
2.2 x I0"7

Relative
Declination(degrees)
23.6
293.2
352.9
58.5
302.3
348.0
91.5
264.3
8.2

54.0
159.5

Inclination(degrees)

Peak Field(oersted)

-27.4
16.6
22.4
-13.0
40.1

50
50
50
50
50
50
50
50
50
50
50

9.7

-52.8
42.7
-11.3
35.7
31.2

Af Demagnetization
Relative
Intensity
Declination(G/cm3)(degrees)
1.5 x I0- 8
1.3 x I0- 7
1.6 x I0- 7
1.8 x I0" 7
1.3 x I0"7
7.4 x I0" 7
1.2 x I0' 7
1.8 x I0- 7
4.4 x I0" 7
7.9 x 10-6
1.6 x I0" 7

339.0
279.3
27.3
55.6
28.1
345.7
285.0
234.6
5.8

68.5
166.2

Inclination(degrees)
20.3
50.9
13.8
4.0

35.3
21.1
13.7
35.5
-18.7
65.8
40.9

SITE 219
TABLE 7Af Demagnetization Results, Hole 219A

Sample7-3,77 cm

14-2,118 cm

Relative
Declination Inclination(degrees)(degrees)

Peak Field(oersteds)

Intensity(G/cm3)

NRM
25
50
75
100
150
200

2.1 x 10-6
1.3x10-6
7.4 x 10-7
4.1 x I0"?
2.8 x I0" 7
2.4 x 10-7
5.7 x 10-7

315.0

-33.3
-31.0
-33.9

NRM
25
50
75
100
150
200

1.1 x 10-5
9.4x10-6
7.9 x 10-6
6.7 x 10-6
5.7 x 10-6
6.0 x 10-6
7.1x10-6

54.0
52.9
68.5
122.9
129.6
47.0
19.5

35.7
51.3
65.8
78.9
64.8
52.6
40.1

348.0
358.3
345.7
0.0
3.8
7.8

9.7

19.7
21.6
0.0

X [ 7-3-77 ] ) Glauconitic
O ["14-2-118] J sandstone

J/Jochert (below Core 219-19) were found in Middle Eocene to
Lower Oligocene sediments (Cores 219-21 to 219-16), andchert was found in older sediments down to the beginningof the Early Eocene; however, such concentrations ofbiogenic silica in the Eocene may partly reflect a much
more widespread, or even global, change in seawaterchemistry (see other Leg 23 Arabian Sea sites; also Heathand Moberly, 1971). Samples from the uniform chalks andoozes of the top 230 meters of the site were analyzed fortrace elements and the upper 100 meters, post-Lower
Miocene sediments, were found to be enriched between
three and tenfold in vanadium and nickel. These traceelements together with zinc and molybdenum (not soughtfor) are believed to indicate an oxygen-poor benthic
environment consistent with deposition in an upwelling
region (McKelvey and Chase, 1966). In accord with thisinterpretation is the relatively high organic carbon content
in the top 100 meters, compared with most of theunderlying sediments, and the presence of pyritic layers andburrows in this interval. Thus, the above rather scantevidence could be interpreted to suggest upwelling near thesite in Tertiary times, especially since the Early Miocene,
although evidence is lacking for the entire Middle Oligocene
to Early Miocene period. The latter period was a time ofvery slow sedimentation at the site, possibly due to strong
near bottom currents. Additionally, from a study of coresand Oceanographic data from the western continental
margin of India, von Stackelberg (1972) detected amarkedly oxygen-poor layer in the sea lying between 150
and 700 meters depth off Cochin. Where this layer impinges
on the sea bed, biogenic silica has undergone solution andbioturbation is lacking except for rare pyritized burrows.
The data of Rao and Jayaraman (1966) also suggest the topof such an oxygen-poor layer off Minikoi occurs at depths
around 200 meters, due to upwelling. The cores from Site
219 indicate that the base of this layer has extended to adepth of at least 1860 meters, assuming no Neogene
subsidence of the site, since the Middle Miocene. Wyrtki(1971, ch. 2) shows a mean dissolved oxygen level of about
2 ml/1 for the sea bed at this site today.
Comparisons with India and the Ninetyeast Ridge

200
Demagnetizing f i e l d (oe.)

Figure 10. Normalized intensity decay curves.
appear to have sunk at mean rates between 18 and 70
m/m.y. (Ladd et al., 1950, 1953,1967).
Evidence of Upwelling

Other conclusions can be made from the sediments
concerning the paleoenvironment of this site. The
paleolatitude in Late Paleocene times, as determined from
paleomagnetic measurements, was about 16°S. This isconsistent with the tropical and subtropical foraminiferal
faunas found at the site. Upwelling occurs today in the
Minikoi region during the northeast monsoon (Rao andJayaraman, 1966), and it is interesting to see whether tracesof earlier upwelling can be found in the sediments.
Phosphorite concretions were found in a core of Early
Eocene age. Rich radiolarian faunas, sponge spicules, andComparisons may also be made with the geology ofIndia and an adjacent DSDP site. The Paleocene shallow
benthonic foraminiferal fauna of Site 219 is similar to thatof the east coast of India, and one species, Discocyclina
ramaraoi Samanta, is otherwise known only from thePondicherry formation. This suggests a marine link with theeast coast of India in Paleocene times. The Eocene
sediments of peninsula India are in part marine, but incontrast to Site 219, chert is unknown in these rocks(Wadia, 1968).
It is also interesting to compare the history of Site 219
on the Laccadive-Maldive Ridge with that of Site 217 on
the Ninetyeast Ridge, which is at the same latitude and on
the same plate (von der Borch et al., 1972). Site 217 has
sunk since Late Campanian times, and today the whole
ridge is free of living coral reefs, whereas, coral atolls exist
within 200 kilometers to the north and south of Site 219,
where the sea bed started to sink in the Late Paleocene or
Early Eocene at latitude 16°S. Colonial corals are

53

SITE 219

temperature dependent, and it would seem that (provided
the Ninety East Ridge did not sink too fast for coral
growth) as the Indian plate moved northwards, it crossed
the critical 20°C isotherm for coral growth between Late
Campanian and Late Paleocene times. The 75 m.y.
reconstruction of McKenzie and Sclater (1971) shows Site
217 to have been at latitude 40° S.
Chert Reflector and Depth to Igneous Basement

combining reflection profiles and soundings, mainly in theregion south of the site, it seems that several of the sea bed
scarps have a NNE trend (Figure 12) consistent with afracture zone origin. A further feature of the reflection
profiles is the way in which the post-chert sediments havefilled in the irregularities in the chert reflector. The uneventhickness of sediment overlying the chert reflector suggests
the influence of bottom currents on their deposition. Thissuggestion is strengthened by the wavy almost dune-likeprofile of parts of the sea bed.

The strong diffuse reflector at this site has been
demonstrated to be Early and Middle Eocene chert while adeeper less distinct reflection is attributable to theshallow-water Paleocene sandstone. No deeper reflections
were discernible on the airgun records so that the true
depth to igneous basement is still unknown. However, anestimate may be made from the results of Francis and Shor
(1966). Their Station 1 detected a 3.85 and a 5.00 km/sec
refractor. They attributed the 3.85 km/sec velocity tovolcanic rock, but from our results it seems certain that
this is incorrect and this refractor is chert or shallow-water
limestones and sandstones. The 5.00 km/sec refractor
probably does represent volcanic rock, however, and lies
over 1500 meters below the bottom of Hole 219A; thisdoes not necessarily exclude the possibility of igneous
basement lying at a shallower depth.
The main feature of the reflection profiles across the site
(Figures 3, 11) is that the strong Eocene chert reflector has
an irregular surface, often with a sawtooth profile. The
steeper parts of the sawtooth have a varying vertical offset
which is generally greater than the present-day sea floor
relief. For instance, just east of the site the chert reflector isdepressed some 1.1 sec (about 1000 m) whereas, thesea bed only shows relief of 250 meters. The profile of thechert reflector suggests that post-Middle Eocene faulting
has occurred, but the lack of any evidence of consistentdip, micro-faulting, or slump structures in the cores does
not support this, although, admittedly, all the Neogene
cores were disturbed by drilling and such structures may
have been destroyed. An alternative explanation is that thechert beds were draped over preexisting rough topography,
the greater relief of which was attributable to the verticaloffset across fracture zones. From the site survey and by

Depositional History
The sedimentary history of Site 219 can, therefore, besummarized as follows. In Late Paleocene time, shallowwater limestones, sandstones, and siltstones were deposited(at least 70 m/m.y.) on a subsiding foundation in water
depths of less than 100 meters. Fresh unaltered detrital
feldspar, zeolite, and montmorillonite in these sedimentssuggest a volcanic provenance, perhaps the Deccan Traps.
Toward the end of the Late Paleocene, the detrital
component decreased and a glauconitic limestone was laid
down. Then in Early Eocene time, the sea bed began to sinkconcurrently with other tectonic events in India (formationof Cambay graben, first Himalayan uplift), and mainly
chalk and ooze were deposited at a slower rate (18 m/m.y.).
Phosphorite concretions in one core suggest local upwellingand nondeposition at this time. Biogenic silica, later tobecome chert, began to accumulate. Fairly constantconditions seem to have been maintained, except for anever decreasing sedimentation rate, until Early Oligocene
time when biogenic silica became scarce in the sediments.
The decrease in biogenic silica seems to have been reflectedby an increase in carbonate. From Early Oligocene to Early
Miocene time, sedimentation was minimal (about 1 m/m.y.)and probably reflects a time when the site was subject tostrong bottom currents. The cause of such currents is
uncertain but may be related to the postulated vigorous
Oligocene circulation due to global climatic cooling which
led to the essential absence of Oligocene sediments at
drilling sites between Australia and New Zealand (Kennett
et al., 1972). A similar regional Paleogene unconformity
appears to exist to the north, east, and south of Madagascar

WEST

Kts.

1000

0900 c/s

0800

EAST_2.

— 3°

Figure 11. Seismic reflection profile obtained by Glomar Challenger during the approach to Site 219 showing the irregularsawtooth shape of the chert reflector and the wavy dune-like nature of the sea bed.

54

SITE 219

REFERENCES

74C

Figure 12. Sea floor scarps deduced from collectedsoundings and from seismic reflection profiles obtained
by Glomar Challenger, Conrad and Oceanographer.£αc/z
long dash denotes one observation of a scarp with thesquare on line (soundings or reflection profile,
respectively) denoting the side on which the scarp facelies. Short dashes represent interpolations between
observations. Oceanographer data courtesy of N.O.A.A.
Atlantic Oceanographic and Meteorological Laboratory,
Miami; Conrad data from cruise Conrad-9 courtesy of
the Lamont-Doherty Geological Observatory.
(Simpson et al., 1972). In post-Early Miocene time, a nannoooze, supplemented by a 20 to 35 percent detrital
component, was deposited at a mean rate of around 15
m/m.y. At first: the ooze contained abundant foraminifera
but with the onset of upwelling they became rarer in thesediments due to solution, probably because the carbonate
compensation depth rose as a consequence of the upwelling(La Fond, 1966). The detrital material may have been
carried to the site in suspension by near bottom currents
and may have originated from the erosion of the Deccan
Traps. Upwelling, which appears to have begun in Middle
Miocene time, continues to the present day. Fresh volcanic
glass is found throughout the Pleistocene sediments as has
been reported by von Stackelberg (1972), who believed it
to be of eolian origin probably from the southeast. Todaythe closest active volcanoes are northwest of Karachi andnear the Andaman islands.

Admiralty Hydrographic Office, 1963. Bathymetric magnetic and gravity investigations, H.M.S. Owen
1961-1962: Admiralty Mar. Sci. Publ. 4.
, 1966. Bathymetric and Magnetic investigations.
H.M.S. Dalrymple 1961-1963: Admiralty Mar. Sci. Publ.
8.
Ewing, M., Eittreim, S., Truchan, M., and Ewing, J. I.,
1969. Sediment distribution in the Indian Ocean: Deep
Sea Res., v. 16, p. 231-248.
Francis, T. J. G. and Shor, G. G., 1966. Seismic refraction
measurements in the northwest Indian Ocean: J.
Geophys. Res., v. 71 (2), p. 427-Φ49.
Gaposchkin, E. M. and Lambeck, K., 1971. Earth's gravity
field to the sixteenth degree and station coordinatesfrom satellite and terrestrial data: J. Geophys. Res., v.
76(20), p. 4855-4883.
Glennie, E. A., 1936. Report on the values of gravity in theMaldive and Laccadive islands: JOHN MURRAY
Expedition (1933-1934) Sci. Repts., v. 1(4), p. 95-107.
Goldberg, E. D. and Arrhenius, G., 1958. Chemistry ofPacific pelagic sediments: Geochim Cosmochim. Acta, v.
13, p. 153-212,
Heath, G. R. and Moberly, R., 1971. Cherts from thewestern Pacific, Leg 7, Deep Sea Drilling Project. In
Winterer, E. L., Riedel, W. R., et al., Initial Reports of
Deep Sea Drilling Project, Volume 7: Washington (U. S.
Government Printing Office), p. 991-1008.
Harbison, R. N. and Bassinger, B. G., 1973. Marine
geophysical study off western India: J. Geophys.,Res. v.
78, no. 2, p. 432-440.
Kennett, J. P., Burns, R. E., Andrews, J. E., Churkin, M.,
Davies, T. A., Dumitrica, P., Edwards, A. R., Galehouse,
J. S., Packham, G. H., and Van der Lingen, G. J., 1972.
Australian-Antarctic continental drift, paleocirculation
changes and Oligocene deep-sea erosion: Nature Phys.
Sci.,v. 239, p. 51-55.
Ladd, H. S., Tracey, J. I., LUI, G., Wells, J. W. and Cole,W. S., 1950. Drilling on Bikini Atoll, Marshall Islands:
International Geol. Cong., Proc. (W. B. Harland, Ed.)
sec. G, pt. 8, p. 38-43.
Ladd, H. S., Ingerson, E., Townsend, R. C , Russell, M. andStephenson, H. K., 1953. Drilling on Eniwetok Atoll,
Marshall Islands: Am. Assoc. Petrol. Geol. Bull., v. 37(10), p. 2257-2280.
Ladd, H. S., Tracey, J. I., and Gross, M. G., 1967. Drillingon Midway Atoll, Hawaii: Science, v. 156 (3778),
p. 1088-1094.
Lafond, E. C, 1966. Upwelling. In Encyclopaedia of
Oceanography, Fairbridge, R. W. (Ed.): New York.
(Reinhold Publ. Corp.), p. 1021.
Laughton, A. S., Matthews, D. H., and Fisher, R. L., 1971.
The structure of the Indian Ocean. In The Sea, Maxwell,A. (Ed.): New York (John Wiley & Sons Inc.), v. 4 (2),p. 543-586.
Loeblich, A. R. and Tappan, H., 1964. Treatise on
Invertebrate Paleontology, Pt. C, Protista (2): Geol. Soc.
Am., v. 2, p. 686.
McElhinney, M. W., 1968. Northward drift of India- examination of recent paleomagnetic results: Nature,v. 217, p. 342-344.
McKelvey, V. E. and Chase, L., 1966. Selecting areas
favourable for sub-sea prospecting; M.T.S. Conf., 2ndAnn. Trans., Exploiting the Ocean, p. 44-60.
McKenzie, D. P. and Sclater, J. G., 1971. The evolution of
the Indian Ocean since the Late Cretaceous: Geophys. J.
Roy. Astro. Soc, v. 25, p. 437-528.

55

SITE 219
Moore, T. C, 1971. Radiolaria. In Tracey, J. I., Jr., Sutton,
G. H., et al., Initial Reports of the Deep Sea Drilling
Project, Volume 8: Washington (U. S. Government
Printing Office), p. 727-748.
Obradovitch, J., 1965. Problems in the use of glauconite
and related minerals for radioactivity dating: Unpubl.
dissertation, Univ. Calif. Berkely.
Odin, G. S., in press. Specificite des datations radiometriques dans les roches sedimentaires: Rev. Geog.
Phys. Geol. Dynamique.
Porrenga, D. H., 1967. Clay mineralogy and geochemistryof recent marine sediments in tropical areas: FysischGeografisch Lab., Univ. Amsterdam, Publ. 9, 145 p.
Purdy, J. W., 1972. The Varian MAT GD 150 for argon
analysis in connection with K-Ar dating: Eclog. Geol.
Helv.,n. 65, p. 317-320.
Rao, L. V. G. and Jayaraman, R., 1966. Upwelling in the
Minicoy region of the Arabian Sea. Current Sci.,v. 35(15), p. 378-380.
Riedel, W. and Sanfilippo, A. 1970. Radiolaria, Leg 4 DeepSea Drilling Project. In Bader, R. G., Gerard, R. D., etal., Initial Reports of the Deep Sea Drilling Project,
Volume IV: Washington (U. S. Government Printing
Office), p. 503-575.
Samanta, B. K., 1967. Discocyclina from the Early Tertiary
sediments of Pondicherry, South India: Micropaleontology, v. 13, no. 2, p. 233-242.
Seibold, E., 1972. Sedimentary regions at continental
margins and in abyssal cones in the Indian Ocean: I.G.C.,
24th, Proc. Sec 8, p. 75-84.

56

Simpson, E. S. W., Schlich, R., Leclaire, L., Girdley, W. A.,
Moore, C, White, S., Valuer, T. L., Muller, C , Zobel, B.,
Sigal, J., Gieskes, J., and Marshall, B. V., 1972. Leg 25
DSDP, western Indian Ocean: Geotimes (November).
Turekian, K. K. and Tausch, E. H., 1964. Barium in deep sea
sediments of the Atlantic Ocean: Nature, v. 201, p. 696.
Vinogradov, A. P., Udintsev, G. B., Dimitriev, L. V.,
Kanaev, V. F., Neprochnov, Y. P., Petrova, G. N., andRikunov, L. N., 1969. The structure of the Mid-Ocean
Rift Zone of the Indian Ocean and its place in the worldrift system: Tectonophys., v. 8, p. 377-401.
von der Borch, C. C, Sclater, J. G., Gartner, S., Hekinian,R., Johnson, D. A., McGowran, B., Pimm, A. C,
Thompson, R. W., and Veevers, J. J., 1972. Deep Sea
Drilling Project, Leg 22: Geotimes (June), p. 15-17.
von Stackelberg, U., 1972. Faziesverteilung in Sedimenten
des indisch-pakistanischen Kontinentalrandes (Arabisches Meer): "Meteor" Forsch-Ergeb., Reihe, C, No.
9, p. 1-73, Berlin, Stuttgart.
Wadia, D. N., 1968. The Geology of India: (McMillan and
Co. Ltd), p. 536.
Wilson, J. T., 1963. A resume of the geology of islands inthe main ocean basins. 1—Atlantic and Indian Oceans:
Univ. Toronto, Sci. Repts. 4.
Woollard, G. P., 1969. Standardisation of gravity
measurements. In Hart, P. J. (Ed) The Earth's Crust andUpper Mantle: A.G.U. Geophys. Mon. 13, p. 283-293.
Wyrtki, K., 1971. Oceanographic Atlas of the International
Indian Ocean Expedition: Washington (National Science
Foundation).

SITE 219

SITE 219

GEOCHRONOLOGICAL AGE

CARBONATE(wt %)
20 40 60 80

LITHOLOGICAL UNITS
Hole
219

Light gray to greenish gray DETRITALSILTY CLAY NANNO OOZE becoming
DETRITAL CLAY RICH NANNO OOZE inlower part. FORAM RICH in upper andlower parts.

II

White FORAM OOZE/CHALK,
upper part.

RICH ina) FORAM NANNO OOZE/CHALKIII White
BIOGENICOOZEb) FORAM RICH NANNO MICARBOOZE/CHALKAc) RAD RICH MICARB NANNOOOZE/CHALK
H200d) NANNO RICH RAD MICARBOOZE/CHALK & CHERTIV Yellow green MICARB FORAM CHALK,MICARB RICH FORAM CHALK/OOZE,LIMESTONE, CHERT and DETRITAL CLAY.
L-250

58

A

SITE 219

CORE

WATER CONTENT (wt.)
POROSITY ( v o l . )80

60 40 20
r^~i

T^T

r

DENSITY
3

(g.cm
1.5

COMPRESSIONALWAVE VELOCITY

)

2.0
*T

1

2

(km.s~ )3
4

SPECIFIC
ACOUSTIC
IMPEDANCEδ
3(10 N.s.m2 4 6 8

THERMAL CONDUCTIVITY
(Wm~

1

1

K' )

T i l l

4

t

50-

100-

T

*

150-

A

200-

250-

J

I

I

L

J

L

J

L

J

I

I

L

I

l

i

l

For explanatory notes see chapter 2.

59

SITE 219

SITE 219
i— >>GEOCHRONOLOGICAL AGE

LU
Q

_i ε

o
GO LU

CO CD

GRAPHICLITHOLOGY

LITHOLOGICAL UNITS

20 40 60 80

< =c
Early

Hole
21 9A
-300

Grayish green LIMESTONE,
GLAUCONITE BEARING or
RICH.

LU

o
LO
Q

Late
o
O

U~)

LU

o

I
<
Q_

I—
u->
LU

-350

(0 O

10

i— I—

11

C 00
Qi
<V T3

b) Yellowish green to darkgreen CALCAREOUS
CEMENTED SANDSTONE, SILTSTONE & CLAYEY SILTSTONE.
Gray to greenish black
CLAYEY SILTSTONE & SILTYSANDSTONE.

S- C
CS (O

13
-400
cα

-450

L.500

60

CARBONATE(wt %)

14*non representative recovery

SITE 219

CORE
250 •

WATER CONTENT (wt.)
POROSITY (vol.)(%)
80 60 40 20

DENSITY
3(g.cπf )1.5 2.0

COMPRESSIONALWAVE VELOCITY_l(km. s2
3

SPECIFIC
ACOUSTIC
IMPEDANCEδ(10 N.s.m2 4 6 8

THERMAL CONDUCTIVITY
(Wm"

3

1

2

1

1

K~ )
3

4

I

I

©

300-

350-

CSD

400-

450-

500-

,

j

For explanatory notes see chapter 2.
61

£

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LITHOLOGY

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8

°

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-^_

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-

Dominant l i t h o l o g y SS: Section 2-25 cm
FORAM RICH DETRITAL SILTY CLAY NANNO OOZE
Composition:
Nannos55%
D e t r i t a l grains
30%
Forams'12%
Volcanic glass
3%
Carbonate needles
Trace

Dominant lithology SS: Section 3-90 cm
FORAM DETRITAL SILTY CLAY RICH NANNO OOZE
Composition:
Nannos60%
Detrital grains
20%
Forams15%
Volcanic glass
5%

1 = y e l l o w i s h gray5Y 7/22 = l i g h t o l i v e gray5Y 5/23 « pale o l i v e
10Y 6/2
4 = moderate o l i v e brown 5Y 4/4
5 - grayish o l i v e
10Y 4/2

r

00.
CΛ| Pseudc

3UjS;

I
Core
Catcher X .

O

60

2&
1

I

T
—i

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2

-r

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/

T
T"
:
- -*—_ 1|_ T(d

DESCRIPTION

Gray FORAM DETRITAL SILTY CLAY RICH NANNO OOZE
Some pyrite streaks occur in the lower part ofthe core.

Gray FORAM RICH DETRITAL SILTY CLAY NANNO OOZE

140

J5
1

40

~"

/ U J

6-15

LITHOLOGIC

140

1

;

Cored Interval:

Color legend:
2
—I]
—12
3
,

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i

25

T

•>~

-

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2

T

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1

140

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T .-A:T"

T •/Core 2LITHOLOGIC DESCRIPTION

—i
—'

Vc r
_L T
.U".'_•
1.0— ~ ^ ~ | T_ — 1 - _,_ • A•
- _L.
_L
—
-r

-

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Hole
FOSSILCHARACTER

50

1 C

z

<
—

219

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-J- . - 1 J
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1 1 1

z

>

8
ribb

LATE 1

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-σ

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- J

>

Site

o

F N R

s

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Cored I n t e r v al.•Core 1

FOSSILCHARACTER

THO. SAF IPLIHole

S i t e 219

o
125
—i
-

— v—

A

CC

5

Shore-based laboratory

results

Color legend:
1 = grayish olive
10Y 4/2
2
greenish yellow
10Y 7/2
3 = l i g h t olive gray5Y 5/2
4greenish black
5GY 2/1
5
moderate olive brown
5Y 4/46
dusky yellow
5Y 6/47
greenish gray5Y 6/18
yellowish gray5Y 7/29
pale olive
10Y 6/2
10
pale greenish yellow
10Y 8/2
11
greenish gray
5GY 6/1
12 = moderate greenish yellow 10Y 7/4

Carbonate
Section 1-38 cm • 68%
Section 1-139 cm = 52%
Section 2-38 cm = 58%
Section 3-40 cm = 60%
Section 4-30 cm = 71%-T

Shore-based laboratory results

Explanatory notes in chapter 2Core
Catchei
Explanatory notes in chapter 2

Section 1-10
Section 2-20
Section 3-40
Section 4-90
Section 5-40

Site

Core

219

3

Cored I n t e r v a l :15-24

Site 219

Hole

Core

4

Cored I n t e r v a l : .

24-33

FOSSILCHARACTERFOSSILCHARACTER

LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTION

Gray DETRITAL SILTY CLAY NANNO OOZE
Lower sections contain some pyrite streaks
and there is a general coarsening of the
detrital fraction.

Gray DETRITAL SILTY CLAY NANNO OOZE
Dominant lithology SS: Section 5-90 cm
DETRITAL SILTY CLAY NANNO OOZE
Composition:
Nannos55%

Dominant lithology SS: Section 4-60 c
DETRITAL SILTY CLAY NANNO OOZE
Composition:
Nannos50%
Detrital grains
35%
Forams10%
Volcanic glass
5%

D e t r i t a l grains
ForamsColor legend:
1 =
2 =
3 =

Color legend:
1 2=
3 =
4 =
5 =

35%
10%

greenish gray
5GY 6/1
l i g h t o l i v e gray 5Y 5/2
pale o l i v e
1OY 6/2

greenish gray
5GY 6/1
l i g h t greenish gray 5G 8/1
pale o l i v e
10Y 6/2
grayish o l i v e
TOY 4/2l i g h t o l i v e gray5Y 5/2

Shore-based laboratory results

Core
Catcher

Carbonate
Section 1-40 cm - 56%
Section 2-40 cm - 59%
Section 3-40 cm = 65%

Explanatory notes in chapter 2

Shore-based laboratory r e s u l t sCoreCatcher
Explanatory notes in chapter 2

Carbonate
Section 2-40 cm = 67%
Section 3-40 cm = 61%
Section 4-40 cm = 64%

Site 219

Hole
FOSSILCHARACTER

Core

5

Cored Interval: 33-42

Site

LITHOLOGIC

219

Hole

Core

6

Cored Interval: 42-51

DESCRIPTION

LITHOLOGIC

Gray DETRITAL SILTY CLAY NANNO OOZE
Most of core badly disturbed.

Gray DETRITAL SILTY CLAY NANNO OOZE
Dominant lithology SS: Section 3-130 cm
DETRITAL SILTY CLAY NANNO OOZE
Composition:
Nannos55%
Detrital grains 35%
Forams10%

Dominant lithology SS: Section 3-120 cm
DETRITAL SILTY CLAY NANNO OOZE
Composition:
Nannos55%
Detrital grains 35%
Forams1 OX
1&2Color legend:
1 - greenish gray2 = l i g h t gray

DESCRIPTION

Color legend:
1 = greenish gray
5GY 6/1
2 = olive gray5Y 5/23 = light gray5Y 6/14very light gray N8

5GY 6/1
5Y 5/2

Shore-based laboratory results
Core
Catchei

Carbonate
Section 1-40 cm = 62%

Explanatory notes in chapter 2

1 to
4

IJ4
1

Λ
4
\
1S
4
~:4
-ll
1 S
4

Shore-based laboratory results
Carbonate
Section 1-40 cm

Explanatory notes in chapter 2
Podocyrtis ampla fasciolata

Cored I n t e r v a l :

51-60

Site

219

Hole

Core 8

Cored I n t e r v a l :N R

5ECTI0,

LITH0L0GY

0.5-

Void

DEI:0RMAT IOfs

METER;F

FOI?AMSZONEDESCRIPTIONAGE

LITHOLOGICHERSFOSSILCHARACTER

o

60-69

LIT;HO.SAM

Core 7FOSSILCHARACTER

NAIMNOS

Site 219

LITH0L0GIC

Gray DETRITAL SILTY CLAY NANNO OOZE

Gray DETRITAL SILTY CLAY NANNO OOZE
Color legend:
1 = very light gray2 - greenish gray

1

N8
5GY 6/1

ly pi

_
1.0—

I-

~-L-"11 .
_
I

2
•

_

~

•

_

330

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ved

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_ "^― j~ ™ '- ~->-j^•
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l

S

CL

lith

s

in

ε

s

c
L

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L

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1

Q.

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s

/

I
1

1

•

cr

Mot. 1& 2

CoreCatcher
Explanatory notes in chapter 2

Carbonate
Section 2-40 cm • 66%

Dis :oas ter

Shore-based laboratory results\TE MIOC ENE

3cm long
pyr. bur.

z -ij-:- ~- - •

Ul

i

-

•

~

.

:

-

_

;

-

;

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-

:

:

.

:

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cr

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/

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5

/

6

Explanatory notes in chapter 2

~

-

-

~

'

.

1)
\/

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1&
2

1

—i

2

3
2 &1
^ 3

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z: >i•~

Core L _Catcher

5GY 6/1
N8
10Y 6/2:

E
E/

Color legend:
1
greenish gray2very l i g h t gray3 = pale o l i v e

o

o
o
o
"1LT oo.T_.T: o"^~: oo— oo-"'- o— oo~z~.'.or:sr:.ozz~s. oL-j^-l-" - ~ - '1- _!_' —
—

Φ

1o
o
o
o
o
o

-

z

Dominant l i t h o l o g y SS: Section 6-105 cm
DETRITAL SILTY CLAY NANNO OOZE
Composition:
Nannos6ffl
D e t r i t a l grains
3ffl
Forams
1ffl

_l_

-ITI

1
X

1 &
2

DESCRIPTION

2
—>T

2

Shore-based laboratory results
Carbonate
Section 2-40 cm = 71%

9Cored I n t e r v a l :

69-78

19

Site

Hole

Co -e

Cored Interval:

1

•JO I

FOSSIL

F

N R

ε

s

Color legend:
1 = l i g h t o l i v e gray2 = very l i g h t gray
3 = green gray:

LITHOLOGY

πri

Gray DETRITAL SILTY CLAY RICH NANNO OOZE

i

1.0—

5Y 5/2N8
5GY 6/1

c

1

2

and

S•

E

_2

res erv

-c

3

O-

UJ

o

Gray DETRITAL SILTY CLAY RICH NANNO OOZE.

.- )

1 &
2

/

_- / i—[_-Jo 2R!

oo_ _1_-L-_1_-1o- -1-__Lo-1_ _1
I

Section 2 contains some p y r i t e streaks. Manycolor bands have mottles which are the colorof the adjoining bands.
Minor l i t h o l o g y SS:
PYRITIC NANNO OOZE
Composition:
NannosPyriteForamsColor legend:
1 = green gray2 = very l i g h t grayooo_ l _ _Lo:i o-1— . 1oooooSection 2-28 cm
50%
38%
12%
5GY 6/1
N8

Remarks:
A depth of 4 meters was only cored, thus
the extra core length recovered indicatesthat sections 3-6 represent duplicationof sediment already cored.

1

=

1

a.

LITHOLOGIC DESCRIPTION_ -1-—1-

CD

3

_l^

-1-

α>.
o

a!

-1—
—1_
-i . L .
- _l_
_1_
T.

Jj

78-82

IT. )

0 . 5 - _l_- J -_l_- L- J--•--J.- 1
1

Many color bands have mottles which are thecolor of the adjoining bands.

DEI 0RMATgg

METER;AGE

DESCRIPTIONSONt

LITHOLOGIC

ZONECHARACTER

LIT HO.SAM

Core

FOSSILCHARACTER

iECTIOlHoleOTIHERS

219

NAI

Site

IOC ENE

-L-

-L

c*

I -t-, -L ,

o

zI

u

- L -_ 1 _- J -_ t
-Lj_-L_1

—
-

o

o
o
o
o
- o
- o
o

O |i

ON

t.

5

I -1- , -L | _- _L_ _l "- o- o
I _1_ _1_ ]'- o

—i

2
,
1

o
o
.7! o
_L
_•-

g

i ~ ^

:
Shore-based laboratory results:i2 & 3
3 & 2
3
H
2

Core
Catche•Explanatory notes in chapter 2

Carbonate
Section 1-40 cm = 74%
X-ray mineralogy: Section 1-45 cm
Calcite"90?
Dolomite1%
Quartz4?
Plagioclase
1%
Mica
3%
Chlorite
λ%

_|_

;

6

t

_•-

-"

I

'z

J)

1 grading
to 2

1

2

o

Core
Catcher

Explanatory notes i n chapter 2

-1-

_L _

_1_

_L -

cc

Shore-based laboratory r e s u l t sCarbonate
Section 1-40 cm = 74%

219

Hole

Core

Cored Interval:

1

ö
o

F

in

N R

c

:TIO

S

RAD

ONE

FOSSILCHARACTER

h
%
c
c3
u

en
LITH0L0GY
•s:

1

-

Core 12LITHOLOGICDESCRIPTION

LITHOLOGICII

Color legend:
1 = green gray
5GY 6/1
2 = very l i g h t gray N8Dominant lithology SS: Section 4-120 cm
FORAM DETRITAL CLAY RICH NANNO OOZE
Composition:
Nannos60%

1&
2

D e t r i t a l grains
Forams1 • green gray2 = very l i g h t gray

±i±i

•E

MM

AbseniMIDDLE C R LATE MIOCEI>

1 pres erved

_1_

-

I

-

X

6

1

)

- '

2
1

)

^i

2
1

)
\
)

-

J i

IL

_L

-

}

!

!

_l_

1 11 1-ij.

;
I i I I1

i

_i_

-:

1 1 I I 1 1 1 11 I I

Comm

=

5GY 6/1
N8

_L

|g

§

5

25%
15%

Color legend:

2

4

DESCRIPTION

Gray FORAM DETRITAL CLAY RICH NANNO OOZE
Pyrite streaks occur in sections 1, 3, 4, 5
and 6. Most color bands have mottles which are
the color of the adjoining bands.

Gray DETRITAL SILTY CLAY RICH NANNO OOZE
Many color bands have mottles which are thecolor of the adjoining bands.

i•391-100

Void

-

t 1

Cored I n t e r v a l :§j

I i -1- | —*—1~:

J
J

219

FOSSILCHARACTER

0.5 —

1

Site

82-91

.SAF PLE

Site

nS
2

)

—<1

)

2
i
1

C

:
Core
Catcher

Explanatory notes in chapter 2

I-'.

Shore-based laboratory results

Shore-based laboratory r e s u l t sCarbonate
Section 1-40 cm - 76%

Core
Catcher
Explanatory notes in chapter 2

Carbonate
Section 2-40 cm = 75%

Site

219

Hole

Core

13

Cored I n t e r v a l :119-128

Site

219

Hole

Core

14

Cored I n t e r v a l :FOSSILCHARACTER
LITHOLOGICDESCRIPTION

LITHOLOGICF

DESCRIPTIONNWhite and gray NANNO RICH FORAM CHALKWhite FORAM OOZE/CHALK

L o c a l l y v a r y i n g t o FORAM NANNO CHALK and
FORAM CHALK/OOZE.

A l t e r n a t i n g ooze and chalk layers (few d e c i meters t h i c k ) c h i e f l y in sections 3-6.

Dominant l i t h o l o g y SS: S e c t i o n 1-130 cm
NANNO RICH FORAM~CHALK
Composition:
Forams70%
Nannos20*
Detrital grains
10%
Color legend:
1 = light blue gray2 - yellow gray3 = white

Dominant l i t h o l o g y SS: Section 4-90 cm
FORAM OOZE
Composition:
Forams92%
D e t r i t a l grains
5%
Nannos3%
Color legend:
1 = white2yellowish gray5Y 7/1
5Y 8/1N9N9
5Y 8/1

Shore-based laboratory r e s u l t sCarbonate
Section 1-100 cm = 932
Shore-based laboratory r e s u l t sCoreCatcher
Explanatory notes i n chapter 2

X-ray mineralogy:
CalciteQuartzMica

Carbonate
Section 1-40 cm = 86X

Explanatory notes i n chapter 2

Section 5-110 cm
98%
156
U

Site

219

Core 15

Cored I n t e r v a l :156-165

Site

LITHOLOGIC

219

Core 16

White FORAM RICH NANNO MICARB OOZE/CHALK
and NANNO MICARB OOZE/CHALK.

White FORAM NANNO 007E/CHALK.

A l t e r n a t i n g hard chalk bands (maximum adecimeter) and s o f t ooze layers (few decimeters) occur. These are r e g u l a r l y spaced.

In sections 3-4 the hard chalk bands are
regularly spaced -vlδ-20 centimeters.

Dominant l i t h o l o g y SS: Section 4-80 cm
FORAM RICH NANNO MICARB OOZE/CHALK
Composition:
Micarb45%
Nannos40&
Forams15%
D e t r i t a l grains 5%

Dominant lithology SS: Section 4-70 cm
FORAM NANNO OOZE/CHALK
Composition:
Nannos573!
Forams30%
Zeolites
6%
Micarb5%
Detrital grains 2%

Explanatory notes i n chapter 2

C7N

165-174

LITHOLOGIC DESCRIPTIONDESCRIPTION

Alternating hard chalk (few centimeters
thick) and soft ooze bands (few decimeters
thick) in sections 2-6.

Color legend:
1 - white

Cored Interval:

Color legend:
1 = white

N9N9Shore-based laboratory r e s u l t s

Shore-based laboratory r e s u l t sCarbonate
Section 1-60 cm = 92%

Carbonate
Section 1-60 cm = 92%

Explanatory notes i n chapter 2

-J

Site

219

Hole

Core

17

Cored I n t e r v a l :174-183

S i t e 219

Core 18

Cored I n t e r v a l :183-192o
LITHOLOGIC

LITHOLOGICDESCRIPTIONDESCRIPTIONWhite FORAM RICH MICARB NANNO OOZE/CHALKWhite RAD RICH MICARB NANNO 007E/CHALK

Lower part of sections 2, 3, 4 and upper partof 5 contain alternate hard chalk and soft
ooze layers.

Alternate hard chalk (up to a meter). Softooze (up to a few decimeters) layers. The
broken layers shown in deformation column
are mainly of chalk. GLAUCONITE BEARINGi n t e r v a l near middle of core.

Dominant lithology SS: Section 1-75 cm
FORAM RICH MICARB NANNO OOZE/CHALK
Composition:
Nannos43%
Micarb
3 0%
Foram
12%
Sponge spicules
8%Radiolarians
7%
Color legend:
1 = white

Dominant l i t h o l o g y SS: Section 5-75 cm
RAD RICH MICARB NANNO OOZE
Composition:
Nannos50*
Micarb30%
Radiolar ians
12*
ForamsSponge spicules

N9

Color legend:
1 = whiteg l a u c o n i t i c bearing layers.

Shore-based laboratory results
Carbonate
Section 2-75 cm = 87%

Explanatory notes i n chapter 2

Shore-based laboratory r e s u l t sCarbonate
Section 1-45 cm = 85%
X-ray mineralogy: Section 1-40 cm
Calcite100*

Explanatory notes in chapter 2

Site

219

Hole

Core 19

Cored I n t e r v a l :Site

192-201

219

Core

20

Cored I n t e r v a l :201-210FOSSILCHARACTER
LITHOLOGICDESCRIPTIONWhite RAD RICH HICARB NANNO CHALK/OOZE.
CHERT bands.

LITHOLOGIC

Thin

White NANNO RICH RAD MICARB OOZE/CHALK
Alternate hard chalk (few centimeters tometers) and soft ooze (few centimeters tometers). Ooze and chalk occur in approximately equal proportions.

A l t e r n a t i n g s o f t ooze (few centimeters) andhard chalk layers (maximum to 1 meter t h i c k )layers. The broken i n t e r v a l s are hard chalkl a y e r s . Chert near bottom.

Dominant l i t h o l o g y SS: Section 3-80 cm
NANNO RICH RAD MICARB OOZE
Composition:
Micarb40%
Radiolarians
26%
Nannos20%
Forams10%
Sponge spicules
4%

Dominant l i t h o l o g y SS: Section 3-75 cm
RAD RICH MICARB NANNO CHALK
Composition:
Nannos45%
Micarb30%
Radiolarians
13%
Forams10%
Sponge spicules
2%
Color legend:
1 - white
2 - yellowish gray

DESCRIPTION

Color legend:
1 = white

N9N9
5Y 7/2•+• (CHERT)(CHERT)

Shore-based laboratory results

Shore-based laboratory results
12 -*- (CHERT)
Carbonate
Section 1-35 cm = 84%

Explanatory notes i n chapter 2Core
Catcher
Explanatory notes i n chapter 2

Carbonate
Section 2-40 cm = 72%

HoleCore 21

Cored I n t e r v a l :210-219

219

Site

Hole

Cored I n t e r v a l : 237-246

Core 24

1

METERSSECTIO

RADS

ORAMS

<IANNOSDESCRIPTIONAGE

LITHOLOGICZONEFOSSILCHARACTER
LITHOLOGY-

1

Orange LIMESTONE and NANNO OOZE
• ! — L - , -*— ,Color l e g e n d :1 = very p a l e orange

1OYR 8 / 2

eservedeservedDESCRIPTION

Site 219

Hole[ Rare ad poor

Common and we

1 Few tocommon

Disc >aster

&.
>>

j

MQ
N 9

5Y 8/1LITHOLOGICCoreCatcheri
P.8-

Color l e g e n d :1white
2 = y e l l o w i s h gray

c
-o

|

Dominant l i t h o l o g y SS: Section 2-130 cm
NANNO RICH RAD MICARB OOZE
Composition:
Micarb45%
Radiolarians
30%
Nannos15%
Forams5%
Sponge s p i c u l e s 5%

•MOD -E EOCENE

Sections 1 , 2, 3 consist of soupy or massive
ooze. White chalk predominates i n section 4.
Several CHERTY i n t e r v a l s near bottom o f core.

servatior fair to qoodF N RWhite NANNO RICH RAD MICARB OOZE/CHALK w i t h
CHERT.

THO.SAM PLE

219

EFORMAT ION

Site
to

Core

25

Cored I n t e r v a l :246-255

LITHOLOGICDESCRIPTIONWhite ZEOLITE MICARB RICH FORAM CHALK
Dominant l i t h o l o g y SS: Section 1-140 cm
ZEOLITE MICARB RICH FORAM CHALK
Composition:
Forams60%
Micarb15*
Zeolites
15%
Nannos10%

Shore-based l a b o r a t o r y r e s u l t sCarbonate
S e c t i o n 2-40 cm = 71%

219

Hole

Core

22

Cored I n t e r v a l :219-228

Site

DEFORMATION

LITHO.SAMPLE

METERSRADSOTHERSNANNOSFORAMSZONELITHOLOGY

LITHOLOGIC

Site

Hole

Core

219

Hole

Core

26

Cored I n t e r v a l :N9
5Y 8/1
10YR 5/4

255-264

Green CHERT fragments i n core catcher.

A A A AA A A A

219

Color legend:
1 = white
2 • yellowish gray3 » moderate yellow brown

DESCRIPTIONA A A ACore
Catcher

MIDDLE EOCENE

AGE

FOSSILCHARACTERSECTION

1

Site

Minor l i t h o l o g y SS: Section 1-145 cm
RAD RICH DETRITAL CLAY
Composition:
D e t r i t a l grains
70*
Radiolarians
20%
Forams10%

23

Cored I n t e r v a l :Color legend:
1 = grayish yellow green

LITHOLOGICDESCRIPTION

5GY 7/2

228-237
Brown MICARB FORAM CHALKFOSSILCHARACTER
LITHOLOGICCoreCatcher

Dominant lithology SS:
MICARB FORAM CHALK
Composition:
ForamsMicarb
D e t r i t a l minerals
Zeolites

Yellow t o green LIMESTONE and CHERTColor l e g e n d :1 = yellowish green
2
greenish yellow

Explanatory notes i n chapter 2

Chalk contains pieces of LIMESTONE (0-30 cm)
and PHOSPHATE concretions. Sediments aresemi-lithified to lithified.

DESCRIPTION

5Y 7/25GY 7/2

Color legend:
1 = dark yellow brown
Explanatory notes in chapter 2

Section l-θ5 cm

10%SS
10YR 4/2

Site

219

Hole

Core 27

Cored I n t e r v a l :264-273

Hole

Site 219

A

Core

1

Cored I n t e r v a l :0-290

FOSSILCHARACTER
LITHOLOGICDESCRIPTION

LITHOLOGIC

Orange to yellow MICARB RICH FORAM OOZE/CHALK
Many of the sand grains are foraminifera, someof the smaller grains are probably also of
foraminiferal origin.

Green to gray FORAM RAD RICH NANNO OOZE,l o c a l l y NANNO OOZE.
Core taken by washing down to 290 meterswith core barrel i n place. Core material
probably represents the composite of t h i s
e n t i r e i n t e r v a l and i s therefore not r e presentative of the l i t h o l o g y at 290 meters.

Dominant lithology SS: Section 3-80 cm
MICARB RICH FORAM OOZE
Composition:
ForamsMicarb85%
15?

Color legend:
1 • pale yellow orange
2 = pale yellow brown
3 • pale yellow orange
4white

10YR 8/4
10YR 6/2
10YR 8/6
N9

5 •
6 •

green yellow
red brown

DESCRIPTION

Dominant l i t h o l o g y SS:
NannosForamsRadiolarians
Diatoms

10Y 7/4
10YR 5/4

273-

DESCRIPTION

Remarks:
The core barrel became stuck in the holeand the sediment probably represents theinterval just above 273 meters. Many of
the foraminifera are benthonic and larger
forms.
Explanatory notes in chapter 2Core
Catcher
Explanatory notes in chapter 2

Cored Interval:

LITHOLOGY

DEFORMATIONRADSNANNOS

Orange FORAM OOZE
Color is yellowish orange.

FORAMSr -r -rZONECore
Catcher

AGE

FOSSILCHARACTER

LITHO.SAMPLE

Core 2Site 219

METERSLITHOLOGICOTHERSSECTION

LITHOLOGY

DEFORMAT ION

Cored Interval:
LITHO.SAM PLE

METERSRADSCore 28

OTHERSSECTIONANNOSFORAMS

ZONE

AGE

Hole
FOSSILCHARACTER

70%
15%
15%
Trace

Color legend:
1 = grayish o l i v e green 5GY 3/2
2 = dusky yellow
5Y 6/43 - moderate o l i v e brown 5Y 4/4
4 = grayish o l i v e
10Y 4/2
5 = pale greenish yellow TOY 8/2
6 = whiteN97 = light
5Y 8/1g
ggreenish grayl oli
10Y 6/2
8 = palelive

CoreCatcherSite 219

Section 1-140 err

FORAM RAD RICH NANNO OOZE
Composition:

290-299

LITHOLOGICDESCRIPTION

There was no core recovery.

Site

219

Hole

A

Core 3

Cored I n t e r v a l :Site

299-308

LITHOLOGIC

219

Hole

A

Core 4

Cored I n t e r v a l :308-317

LITHOLOGICDESCRIPTIONDESCRIPTION

Yellow and gray LIMESTONEGreen and gray LIMESTONE

Grayish yellow and greenish gray LIMESTONE
containing forams, molluscan shell fragments.
Layers glauconite r i c h and bearing. Shallowwater benthics and larger forams abundant.

Yellowish green and gray LIMESTONE contains
medium to coarse sand size calcareous materialbound by calcareous cement.
Parallel and cross-lamination common, burrow
structures present. Large mollusk fragments
noted.

Color legend:
1 = grayish yellow
5Y 8/42 = grayish yellow green— 5GY 7/2
3 • dark yellowish orange 10YR 6/6
4 = greenish gray
5G 6/1

Color legend:
1 • grayish yellow green
2 = yellowish gray

5GY 7/2
5Y 7/2

1 to
2Explanatory notes in chapter 2

Shore-based laboratory r e s u l t sCarbonate
Section 3-34 cm = 86%

Explanatory notes in chapter 2

Core

5

Cored Interval:Site317-326

219

Hole

Core

7

Cored I n t e r v a l :335-344FOSSILCHARACTER
LITHOLOGIC

LITHOLOGICDESCRIPTIONGreen CALCAREOUS CEMENTED GLAUCONITE RICH
SANDSTONE
Grain size varies from medium to coarse.
Rare horizontal lamination and possibly crosslamination is present in section 3. Burrow
type structures and thick walled mollusk
fragments are in evidence. Varies significantly
in induration from soft to very hard.

Green GLAUCONITE RICH LIMESTONE
Abundant benthic f o r a m i n i f e r a , ostracods,bryozoans.
Grains range from coarse to very coarse sandsize. Fragments o f shells and shallow-watermollusks were noted.
Color legend:
1 = pale blue green

5BG 7/2

Color legend:
1 = grayish green
2 - pale blue green

Shore-based laboratory results

Clinoptilolite

Site

219

Section 2-40 cm

Section 2-80 cm
89%
8%

3%

Cored I n t e r v a l : 326-335

LITHOLOGICDESCRIPTIONGreen CALCAREOUS CEMENTED GLAUCONITE RICH
SANDSTONE overlain by LIMESTONE.
Grains of very coarse sand s i z e . Parallel andoblique lamination noted. Shell fragments
present also abundant benthic f o r a m i n i f e r a .
Color legend:
1 = grayish yellow green

5GY 7/2

Shore-based laboratory results
Carbonate
Section 1-80 cm = 73%

Explanatory notes i n chapter 2

5G 5/25BG 7/2

Shore-based laboratory results
Carbonate

Carbonate
Section 2-75 cm = 75%
X-ray mineralogy:
Calcite'Plagioclase

DESCRIPTIONCoreCatcher
Explanatory notes in chapter 2

Site

219

Hole A
FOSSILCHARACTER

Core

8

Cored Interval:

Cored Interval:

344-353353-362

FOSSILCHARACTER
LITHOLOGIC DESCRIPTION:

LITHOLOGICGreen SANDSTONE, SILTY SANDSTONE, SILTSTONE
and SILTY CLAY
The sandstone varies from semi-lithified tolithified. In addition to a dominance of
detrital grains, pelecypod, foraminifera,
ostracods, red algae, bryozoan and belemnite
fragments are present.

Green GLAUCONITE BEARING SILTSTONE and
SANDSTONE.
The siltstone is laminated and locally biogenous. The sandstone is biogenous andcontains large pelecypod and red algae
fragments, etc. Some of these are glauconitized.

Minor l i t h o l o g y SS: Section 5-100 cm
CALCAREOUS CEMENTED SILTY CLAYSTONE
Composition:
D e t r i t a l minerals
95?
Sponge spicules
5*
Glauconite
Trace
Radiolarians
Trace

Minor litholoαy SS: Section 1-140 cm
SILTY CLAY
Composition:
Detrital grains
90%
Sponge Spicules
10%

Color legend:
1 • grayish green
2 = pale green

Color legend:
1 =' grayish green
5G 5/22 = pale yellowish green 10GY 7/2
3 = light bluish gray5B 7/15G 5/210G 9/2

Remarks:
20% of d e t r i t a l grains are calcareous
particles.

core '.-.::.... _'._Catche**- \Explanatory notes in chapter 2

DESCRIPTION

Shore-based laboratory results
Carbonate
Section 3-43 cm = 22%Core
Catcher
Explanatory notes in chapter 2

Site

219

Core

10

Site

Cored I n t e r v a l : 362-371

219

Hole

A

Core

12

Cored Interval :FOSSILCHARACTERFOSSILCHARACTER
LITHOLOGIC

LITHOLOGICDESCRIPTION

Gray SANDY SILTSTONE, SILTSTONE and SILTY
CLAYSTONE.

Gray SILTSTONE, SANDY SILTSTONE, SILTYSANDSTONE and dark gray CLAYEY SILTSTONE and
CLAYSTONE.

Strata are horizontally laminated.

Burrow structures and pelecypod shell fragments
are common.

Minor l i t h o l o g y SS: Section 2-142 cm
SANDY SILTSTONE
Composition:
Quartz70s;
Feldspars
3 OX
Color legend:
1 = greenish gray2 = dark green gray3 = bluish white
4 = greenish black
5 = white

DESCRIPTION

Minor l i t h o l o g y SS: Section 5-59 cm
SILTY CLAYSTONE
Composition:
Detrital minerals
100?

5G 6/1
5G 4/15B 9/1
5G 2/1N9

Minor lithology SS: core catcher
GLAUCONITIC SILTY CLAYSTONE
Composition:
D e t r i t a l minerals
70%
Glauconite
30%
Color legend:
1 • dark gray2
greenish gray3
dark greenish grayCore
CatcherCore

11

Cored I n t e r v a l :F

METERSSECTIO

THERS

ANNOS

RADS

ORAMS

AGE

ZONE

FOSSILCHARACTER
LITHOLOGY371-380

THO.SAM PLE

A

Hole

EFORMAT ION

Site 219

LITHOLOGIC DESCRIPTION

-•

N R
Void

Gray CLAYEY SILTSTONE and greenish black
SANDY SILTSTONE.

0.5-

1

1

90

Dominant l i t h o l o g y SS: Section 1-90 cm
CLAYEY SILTSTONE
Composition:
D e t r i t a l grains
99%
Nannos and Zeolites
Trace-rEEEz^_t-_ :' E-E~

2

2;:

Sections 2 and 3 are traversed by c a l c i t eveins.

i

Color legend:
1 = greenish gray2 - dark greenish gray
3 = greenish black

5G 6/1
5G 4/1
5G 2/1* c a l c i t e vein
Shore-based laboratory results
3

SiSβ

Abse

Abse

3

Core
Catcher
Explanatory notes i n chapter 2

SBSi

CC

Carbonate
Section 2-47 cm = 2%
X-ray mineralogy: Section 2-45 cm
Calcite3%
Plagioclase
33%
Montmorillonite 49%
Phillipsite
15%

Core
Catche1
Explanatory notes in chapter 2

G G
G Gi
G G

N2
5GY 6/1
5GY 4/1F

RADS

OTHERSFORAMSNANNOSAGEo

13

LITHOLOGY

N R

LITHOLOGIC

Void
0.5i

1
1.0-

Site

Cored I n t e r v a l : 387-396
DEFORMATIONCore

LITHO.SAMPLEA

FOSSILCHARACTER

METERSHoleSECTION

Site 219

LATE PALEOCENE

ö.

219

Hole

A

Core 14

Cored I n t e r v a l : 402-411

DESCRIPTION

LITHOLOGIC

Black and gray SANDSTONE, SILTSTONE andSILTY SANDSTONE

Horizontal and cross-lamination.

Lamination, cross-bedding, graded bedding,load casts, convolute bedding and burrows
are common. Calcite veins are present in
Sections 1 and 5.

5G 5/2
1 to
2

AbsentAbsentAbsent-G

Shore-based laboratory results
1

Large molluscan shells and shell fragments
are common in many beds.
Color legend:
1 = olive black
2 = greenish black
3 = greenish gray4 = dark greenish gray5 = o l i v e gray
6 = very dusky purple red
7
l i g h t greenish grayCarbonate
Section 2-60 cm = 1%

2

core
tcher

DESCRIPTIONGreen CLAYEY SILTSTONE, CLAYSTONE, SILTYSANDSTONE and SANDSTONE.

Color legend:
1 » grayish greenoAbsent-J
00

X-ray mineraloqy: Section 2-60 cm
Calcite9%
Plagioclase
12%
Montmorillonite 64%
Phillipsite
13%
Anal c i t e
1%
AnataseIX

5GY 2/1
5G 2/15GY 6/1
5GY 4/1
5Y 4/1
5RP 2/2
5G 8/1Ca

Explanatory notes i n chapter 2

Shore-based laboratory results
Carbonate
Section 3-60 cm - 37%
Grain size:
Sand
Silt
Clay
Explanatory notes i n chapter 2

Section 3-60 cm
22%
33%
45%

SITE 219
DENSITY (g.cm- 3 )- ^ GRAPE
OSection Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)Syringe Sample
80
60
40
20

219-1
CM

SECTION 1

hθ
0

—1
-25

— 2

|

o

-50

00
<C

— 4

<c
<c
-75
<C
al
cr>
o

— 5

<C

<c
<c
Q.

<c
a:
CD
O

— 6
-100

:

— 7

-125

— 9•
CC
•150

For Explanatory Notes, see Chapter 2

79

SITE 219
3

DENSITY (g.cm- )-N/ GRAPEo Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)ΔSyringe Sample
80
60
40
20

219-2
SECTION 1
CM
-0

0

—1
~25

-50

r—4

-75
r

|

— 6
-100

—7

,, ,Q

—

-125

9•

CC
150
For Explanatory Notes, see Chapter 2

80

SITE 219
DENSITY (g.cm- 3 )^ GRAPE
Q Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)Syringe Sample
80
60
40
20

219-3
SECTION 1
CM
-0

0

—1
-25

,

o

-50

-75
—5

—— 6
-100

—7

—8

-125

CC
150
For Explanatory Notes, see Chapter 2

81

SITE 219
DENSITY (g.cm-3)^ GRAPEα Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)Syringe Sample
80
60
40
20
0

219-4
SECTION 1

-25

\-2

1-3

-50

1-4

-75

1-5

CD
O
O
OL.

O

r-6
-100

1-7

1-8

•125

\-9

cc
-150

For Explanatory Notes, see Chapter 2

82

SITE 219

DENSITY (g.cm-3)^ GRAPED Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)Syringe Sample
80
60 40
20
0

219-5
CM

SECTION 1

hθ

_1
-25

—2

—3

-50

-75

—5

-100

-125

—9
CC
150

For Explanatory Notes, see Chapter 2

83

SITE 219
DENSITY (g.cm- 3 )<-v, GRAPEO Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)Syringe Sample
80
60
40
20

219-6
CM
-0

SECTION 1

0

—1
-25

t\

rt|

— 3

-50

—4

-75
c

|

— 6
-100

—7

—8

-125

CC
150

For Explanatory Notes, see Chapter 2

84

SITE 219
3

DENSITY (g.cm- )~ GRAPEo Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt X)
ΔSyringe Sample
80
60
40
20

219-7
CM

SECTION 1

2

hθ
0

—1
-25

—2

— 3

-50

— 4

-75
— 5

— 6
-100

—7

-125

— 9•

CC
150
For Explanatory Notes, see Chapter 2

85

SITE 219
DENSITY (g.cm-3)~ GRAPEoSection Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)80

ΔSyringe Sample
60
40
20

219-8
SECTION 1
CM

0

—1
-25

—2

*3

a

J

-50

CQ

<C

<C
<C

-75

•x.

ex.

<C
—- 5

CD
O

O

α_
o
— 6
-100

—7

-125

CC

_
150

For Explanatory Notes, see Chapter 2

86

SITE 219
DENSITY (g.cm-3)~ GRAPEo Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)80

Syringe Sample
60
40
20

0

—1

—2

—3

—5

—7

— Q.

CC

For Explanatory Notes, see Chapter 2

87

SITE 219
DENSITY (g.cm-3)^ GRAPE
DSection Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)80

Syringe Sample
60
40
20

219-10CM-0SECTION 1

0

—1
-25

—3

-50

LU

CO

—4

-75
—5

CD
O
O

m
GL.

O

—6
-100

—7

—8

-125

—9
CC
150

For Explanatory Notes, see Chapter 2

SITE 219
3

DENSITY (g.cm- )-v/ GRAPE
α Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)ΔSyringe Sample
80
60
40
20

219-π
CM

SECTION 1

hθ
0

—1
-25

—2

— 3

-50

-75
— 5

™* 6
-100

— 7

-125

— 9•
CC
150
For Explanatory Notes, see Chapter 2

89

SITE 219
DENSITY (g.cm- 3 )^ GRAPEα Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)ΔSyringe Sample
80
60
40
20

219-12
SECTION 1
CM

2

0

-25

—2

—3

-50

OQ

—4

-75
<£.
cxi
CD
O

—5

O
Q-

—6
-100

—7

-125

— 9
CC
150

For Explanatory Notes, see Chapter 2

90

1

SITE 219
DENSITY (g.cm-3)'v GRAPEo Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)80_

Syringe Sample
60
40
20

0

-I

—2

—3

—4

—5

—6

—7

—8

—9
CC

For Explanatory Notes, see Chapter 2

91

SITE 219
DENSITY (g.cm-3)^ GRAPEα Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)80

Syringe Sample
60
40
20

219-14
SECTION 1
CM

0

—1
-25

—2

-50

—4

-75
—5

—― 6
-100

—7

-125

— Q.
CC

150
For Explanatory Notes, see Chapter 2

92

SITE 219
DENSITY (g.cm-3)•~ GRAPE
oSection Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)80

Syringe Sample
60
40
20

219-15CM

SECTION 1

hθ

0

-25

—2

—3

-50

—4

-75
—5

— 6

-100

—7

—8

-125

— 9•

cc
150
For Explanatory Notes, see Chapter 2

93

SITE 219
3

DENSITY (g.cm- )^ GRAPEO Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)Syringe Sample
80
60
40
20

219-16CMSECTION 1

hθ
0

—1
-25

—2

—3

-50

—4

-75
—5

— 6
-100

—7

-125

— 9•

CC
150

For Explanatory Notes, see Chapter 2

94

SITE 219
DENSITY (g.cm- 3 )~ GRAPEo Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt JS)
Syringe Sample
80
60
40
20

219-17CMSECTION 1

hθ
0

—1
-25

—2

—3

-50

—4

-75
|

çr

—6
-100

—7

—8

-125

—9
CC
150

For Explanatory Notes, see Chapter 2

95

SITE 219
DENSITY (g.cm-3)^j GRAPE
α Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)80

Syringe Sample
60
40
20

219-18CMSECTION 1

2

hθ

0

—1
-25

—3

-50

—4

-75
—5

<

I

— 6
-100
f - I

—7
\

-125
e ? π

— 9•

CC
150
For Explanatory Notes, see Chapter 2

96

SITE 219
3

DENSITY ( g . c m - )<~^> GRAPEα S e c t i o n Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)Syringe Sample
80
60
40
20

219-19CM

SECTION 1

hθ
0

—1
-25

—2

—3

-50

-75
—5

— 6
-100

|

It |

-t

-125

- 9

CC

150
For Explanatory Notes, see Chapter 2

97

SITE 219
3

DENSITY (g.cm- )^ GRAPEα Section Mean
1.0
1.5
2.0
2.5

80

WATER CONTENT (wt %)SyHnge Sample
60
40
20

219-20SECTION 1

0

µ•i
-25

h-2

h-3

-50
éut

1-4

-75

1-5

h-6
-100

1-7

125

1-9
cc
-150

For Explanatory Notes, see Chapter 2

98

SITE 219

DENSITY (g.cm-3)^ GRAPE
DSection Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)ΔSyringe Sample
80
60 40
20 0

219-21SECTION 1

CM

i

—1
-25

— 2

—3

-50

I T

V

—•4

-75

—5

-4
""•"* 6

-100

—7

-125

cc
150

II

L.

For Explanatory Notes, see Chapter 2

99

SITE 219
DENSITY (g.cm-3)*N, GRAPE
α Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)80.

Syringe Sample
60
40
20

219-25SECTION 1

0

i

-25

—2

—3

-50

—4

-75
—5

— 6
-100

—7

—8

— 9•

CC

For Explanatory Notes, see Chapter 2

100

SITE 219

DENSITY (g.cm-3)^ GRAPEO Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)Syringe Sample
80
60 40
20 0

219-26CM-0

SECTION 1

-1
-25

—2

—3

-50

—4

-75

—5

-100

—7

-125

—

9•

> .

CC
150

>«

VI!

For Explanatory Notes, see Chapter 2

101

SITE 219
DENSITY (g.cm-3)^ GRAPED Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)80

ΔSyringe Sample
60
40
20

219-27CM-0

SECTION 1

0

—1
-25

-50

—4

-75
—5

h•M

— 6

1,
-100

IV

—7

-125

I
— 9
CC

150

For Explanatory Notes, see Chapter 2

102

SITE 219
DENSITY (g.cm- 3 )^j GRAPE
D Section Mean
1.0
1.5
2.0
2.5

CM

WATER CONTENT (wt %)Syringe Sample

80

60

40

20

219A-1SECTION 1

hθ
0

-25

— 3

-50

— 4

-75

— 6
-100

— 7

-125

— 9.
CC

150

For Explanatory Notes, see Chapter 2

103

SITE 219
DENSITY (g.cm-3)^ GRAPEα Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)80•

ΔSyringe Sample
60
40
20

219A-3CM

SECTION 1

hθ

0

1

-25

—2

— 3

-50

—4

-75
—5

—6
-100

—7

-125

— 9•
CC

150
For Explanatory Notes, see Chapter 2

104

SITE 219
DENSITY (g.cm-3)~ GRAPEα Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt JS)
80

Syringe Sample
60
40
20

219A-4CM

SECTION 1

2

hθ

0

—1
-25

—2

>
-50

CO

<:

CQ

<z
-75
III

r

α_

CS

<c
a:

o

o

CD

o_

o
r-6
-100

-125

— 9•
CC

150
For Explanatory Notes, see Chapter 2

105

SITE 219

^j GRAPE
1.0

DENSITY (g.cm-3)
α Section Mean
1.5

2.0

WATER CONTENT (wt %)Syringe Sample
80
60
40
20

219A-52.5
CM-0

SECTION 1

0

— 1
-25

— 2

i

— 3

-50

-75
|

r

— 6
-100

-125

—

l>~

9•

CC
-150

For Explanatory Notes, see Chapter 2

106" f i -,

SITE 219
DENSITY (g.cm-3)"ss GRAPEQ Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)Syringe Sample
80
60
40
20

219A-6CMSECTION 1

hθ
0

-25

— 2

— 3

-50

— 4

-75

— 5

-100

— 7

-125

—

9•

CC

150

I

For Explanatory Notes, see Chapter 2

107

SITE 219
DENSITY (g.cm-3)^ GRAPE
Q Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)ΔSyringe Sample
80
60
40
20

219A-7CMSECTION 1

hθ
0

— 1
-25

— 2

— 3

-50

— 4

-75

— 5

-100

— 7

— 8

-125

— 9
CC
150
For E x p l a n a t o r y N o t e s , see Chapter 2

108

SITE 219
3

DENSITY ( g . c m - )< NS GRAPEα S e c t i o n Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt X)
ΔSyringe Sample
80
60
40
20

219A-8CMSECTION 1

hθ
0

:
f
*

—1

•

-25

—2

:

-50

CO

— 4

•

"

<c
-75

O-

<c
CC

o
o
Q-

o
— 6
-100

—7

-125

K
— 9•
CC

150
For Explanatory Notes, see Chapter 2

109

SITE 219

÷×, GRAPE
1.0
1.5

DENSITY ( g . c m - 3 )α Section Mean
2.0
2.5

WATER CONTENT (wt %)ΔSyringe Sample
80
60
40
20

219A-9SECTION 1

0

r-1
-25

h-2

r-3

-50

r-4

•75

h-5

r-6
-100

r-7

h-8

-125 \

r-9•

CC
-150

For Explanatory Notes, see Chapter 2

110

SITE 219

DENSITY (g.cm-3)^j GRAPE
Q Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)Syringe Sample
80
60 40
20 0

219A-10CMSECTION 1

h-o

H25

h-3

h50

h-5

-6
h i 00

-7

—

9•

CC
150

For Explanatory Notes, see Chapter 2111

SITE 219
DENSITY (g.cm-3)^ GRAPEo Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)Syringe Sample
80
60
40
20
0

219A-11CMSECTION 1

hθ

-25

-50

-75
— 5

— 6
-100

— 7

-125

— 9
CC
150
For E x p l a n a t o r y N o t e s , see Chapter 2112

SITE 219
DENSITY (g.cm-3)~ GRAPE
αSection Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)ΔSyringe Sample
80
60
40
20

219A-12CMSECTION 1

hθ
0

i

t

-25

—2

^o

amm

-50

i—4

-75

—5

—6
-100

—8

-125

h-9•
CC
150
For Explanatory Notes, see Chapter 2

113

SITE 219
3

^ GRAPE
1.0
1.5

DENSITY ( g . c m - )α Section Mean
2.0
2.5

WATER CONTENT (wt %)ΔSyringe Sample
80
60
40
20

.

219A-13CMSECTION 1

2

hθ
0

•i

-25

—3

-50

CQ

—4

-75

Q.

<c

— 5

CD
O

O

rc

Q_

— 6
-100

—7

-125

— 9•
CC

150

For Explanatory Notes, see Chapter 2

114

SITE 219
DENSITY (g.cm-3)^ GRAPE
0 Section Mean
1.0
1.5
2.0
2.5
WATER CONTENT (wt %)80

ASyringe Sample
60
40
20

219A-14CM-0SECTION 1

0

-25

—2

—3

-50

—4

-75
—5

-–

-100

—8

•"~" 9

F

-125

•

CC
150

For Explanatory Notes, see Chapter 2115