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8/15/2019 Calcareous Nannoplankton Biostratigraphy and Stratigraphic Correlation of the Mesozoic and Cenozoic Sequences …
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PROCEEDINGS INDONESIAN PETROLEUM ASSOCIATION
Tenth Annual Convention, May 19 81
CALCAREOUS NANNOPLANKTON BIOSTRATIGRAPHY AND STRATIGRAPHIC
CORRELATION OF
THE
MESOZOIC AN D CEN OZOIC SEQUENCES IN
CENTRAL , SOUTHER N, AND EASTERN TAIWAN
Wen-Rong Chi
*)
ABSTRACT. During the past three decades, biostrati-
graphy and stratigraphic correlation were studied in
Taiwan with framework mainly based onForaminifera.
Recently, a new biostratigraphic tool, calcareous
nannofossil, has been introduced and successfully
applied to biostratigraphy, stratigraphy, and oil
exploration here.
Th e lithology in central and southern Taiwan i s
characterized b y facies changes and the lack of distinc-
tive marker horizons, especially in the Tainan and
Kaohsiung areas. I t is very difficult t o subdivide these
sequences and make correlations based on the litho-
stratigraphic study alone. Fortunately, most of the
sediments are rich in nannofossils, and
it
is now
possible t o solve the above problems.
In this paper so me very encouraging results obtained
from th e sediments of central and sou thern Taiwan are
Ruc inolith us irregularis
Fasciculithus tympaniformis
Heliolithus kleinpelli
Discoaster mohleri
Heliolithus riedeli
Sphenolithus distensus
Sphenolithus ciperoensis
Triquetrorhabdulus carinatus
Helicosphaera kamptneri
Sphenolithus belimnos
Helicisphaera ampliaperta
Sphenolithus heteromorphus
Cyclicargolithus floridanus
Discoaster variabilis
Discoaster quinqueram us
Ceratolithus acutus
Re iculogen estra pseu doum bilica
Cyclococcolithina macintyrei
Pseudoemiliania lacunose
(a) Coccolithus doronicoides
(b)
Small
Gephyrocapsa
c)
Pseudoemiliania lacunosa
Gephyrocapsa oceanica
presented. A total of
24
calcareous nannoplankton
datums and 20 zonations have been recognized and
proposed from the sediments
of
the studied areas, the
zona tions listed as follows in ascending ord er:
Based on these data, not only stratigraphic correla-
tions can be made among the sections and areas, but
also can be understood their stratigraphic relations
with the rest of Taiwan. Furthermore, the Oligocene/
Miocene, Miocene/Pliocene, Pliocene/Pleistocene
boundaries can be recognized as well.
There are three unconformities that have been
recognized in the Peikang area, and one ih the coastal
Range, eastern Taiwan. These data also provide basis
for the interpretations of the geohistory and the
tectonic movement of central, southern, and eastern
Taiwan.
Early Cretaceous
one
Zone
- - -
-
-
Zone
Zone
Zone
Zone
Zone
Late Paleocene
1
Oligocene
Early Miocene
Middle Miocene
Zone
Zone
Zone
Zone
Zone
Zone
Zone
Zone Late Miocene
1
3
Early Pliocene
one
Zone
Zone - -
-
Late Pliocene
Zone
Subzone
Subzone
Subzone
Zone
- -
-
- -
-
- - arly Pleistocene
Middle Pleistocene
- - -
- -
-
--
*
Chinese Petroleum Corp.
© IPA, 2006 - 10th Annual Convention Proceedings, 1981sc Contents
Contents
Search
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346
INTRODUCTION
During the past three decades, biostrati-
graphy and stratigraphic correlation were
studied in Taiwan with framework mainly
based on benthonic and planktonic Foramini-
fera. Recently, a new biostratigraphic tool,
nannofossils has been introduced and success-
fully applied to biostratigraphy, stratigraphy,
and oil exploration in both the surface and
subsurface sections. The lithology in central
and southern Taiwan is characterized by facies
changes
and lack of distinctive marker bio-
horizons, especially in the Tainan and Kaoh-
siung areas. It is not only very difficult to
subdivide these sequences and make the strati-
graphic correlations among the sections and
basins, but also very difficult to understand
the relations between northern and southern
Taiwan based only on lithostratigraphic study.
Fortunately, most of the sediments are rich in
nannofossils, and it is now possible to solve
the abo ve problems.
Tectonically, the more than 10,000 meters
thick sediments in Taiwan can be spearated
into three terrains: the backbone Central
Range, the Coastal Range in the east, and the
Coastal Plain an d Foothills Region in th e west.
Among them, the last one can be further sub-
divided int o several units: from north t o sou th,
the Kuanyin Shelf, the Hsinchu Basin, the
Miaoli Swell, the Taichung Basin, the Peikang
Shelf, the South Taiwan Basin including the
Tainan and Kaohsiung areas, and the Hengchun
Peninsular (Fig.
2).
The total thickness of the
Tertiary a nd Quaternary in the Western Coastal
Plain has been measured
and estimated by
Schreiber and others (Schreiber, 1965;Chang,
1968, Chou, 1965; Meng,
et al.,
1969). It is
approximately 4300 m below the Kuanyin
Shelf, 7000 9000 m in the Hsinchu Basin,
65 00 00 0 m below the Miaoli Swell, 7500
100,000 m in the T aichung Basin, 1500 2100
m below the Peikang Shelf (Bosum, et al.,
1970). In the South Taiwan Basin, the thick-
ness of the Neogene sediments, becoming
thicker from north to south are at least more
than
5500
m in the Tainan region (Bosum, et
al., 1970).
In this pap er, the biostratigraphy
,
onations,
and stratigraphic correlation will be discussed
in detail based on calcareous nannoplankton
fossils from the sediments of the Taichung
Basin, the Peikang Shelf, the So uth Taiwan
Basin, the Hengchun Penisular , and the Eastern
Coastal Range. The geohistory, the paleo-
environm ent, and the tectonic significance are
also briefly summ arized.
STRATIGRAPHIC RECORDS OF THE CAL-
CAREOUS NANNOFOSSILS
A total of sixty-nine sections of central,
sou ther n, and eastern Taiwan have been selected
for this study, Among them, five sections
belong to the Taichung Basin, twenty sub-
surface sections belong to the Peikang Shelf
twenty-five sections belong to th e so uth Taiwan
Basin, three section belong to the Hengchun
Peninsula, and sixteen sections belong to the
Coastal Range.
Generally, the ages of the sediments from
the study areas range from Mesozoic Aptian
(about 100 M.Y.) to Cenozoic Pleistocene 0.5
M.Y.). The nannofo ssil records are sum marized ,
from north to so uth, as follows:
1.
Taichung Basin
The Taichung Basin is located in the central
part of w estern Taiwan. A total of five sections
are studied, including the Shuiliutung, Peikang-
chi, Takeng, Tsukeng, and Hoshe sections. The
sedimentary sequence ranges from Oligocene to
Late Miocene.
Nannofossils are rare in the Oligocene sedi-
ments but are abundan t in the Early and M iddle
Miocene.
Sphenolithus ciperoensis
Bramlette
and Wilcoxon, Dictyococcites bisectus (Hay,
Mohler, and Wade),
Zygrhablithus bijugatus
(Deflandre) are found from the Shuichangliu
Formation or the Tsukeng Formation and the
basal part of the Takeng Formation (Ho, et al.,
1956). Therefore, this interval can be assigned
to the Late Oligocene in age. However, nanno-
fossils become rare to absent in the remaining
part of the Takeng Form ation, which is
characterized by containing shallow or paralic
sediments, The lower part of the Shuilikeng
Form ation contains well preserved nannofossils
of high diversity. Detailed zonation can be
proposed. The Early Miocene indicators
Tri
quetrorhabdulus carinatus Martini, Discoaster
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34 7
druggii Bramlette and Wilcoxon, Sphenolithus
beleinnos
Bramlette and Wilcoxon, and
Heli-
cosphaera ampliaperta
Bramlette and Wilcoxon
have been commonly found from the sequence
of the Early Miocene interval. The well
preserved, Middle Miocene associations of
high diversity have also been recovered from
the middle part of the Shuilikeng Formation,
representing the Middle Miocene Sphenolithus
heteromorphus Zone, Cyclicargolithus
Jlori
danus Zone, and Discoaster variabilis Zone.
The important species are Sphenolithus hetero-
morphus Deflandre, Cyclicargolithus floridanus
(Roth and Hay), and Discoaster bollii. However,
up to the upper part of the Shuilikeng Forma-
tion, the diversity becomes much less, and the
suggested ages are based
on
only several species.
At the top part of the Shuilikeng Formation,
nannofossils become abundant again, represent-
ing a Late Miocene
Discoaster quinqueramus
Zone. The assemblages are composed of Dis-
coaster quinqueramus Gartner Sphenolithus
abies Deflandre, and Reticulofenestra pseudo-
umbilica (Gartner).
The age of the so-called “Tsukeng Forma-
tion”, characterized by the occurrence of
Discocyclina
and
Nummulites,
was regarded
as Miocene (Ho, 1961) or Eocene (Hashimoto
and Kurihara, 1974; Hashimoto 1979). How-
ever, because a few specimen of Sphenolithus
ciperoensis
Bramlette and Wilcoxon have been
found, the age may be assigned
to
within the
Late Oligocene. F urthermore , quite frequently,
Crataceous, Paleocene, and Eocene secondary
fossils have also been found accompanying
the assemblage. Therefore, the Discocyclina
fossils are believed to be derived from the
Peikang Basement High, southwest of the
Taichu ng Basin.
2. Peikang
Shelf
(Massif)
The Peikang Shelf is located bwtween the
Choshuichi and Chiayi city on the Western
Coastal Plain of central Taiwan. Its existence
has been known from the reconnaissance
seismic, gravity, and aeromagnetic surveys
and it has been recognized and proved in the
drilling of many wildcat wells by the Chinese
Petroleum Corporation during the past decades.
There are a total of
20
subsurface borehole
sections tha t have been studied fro m the
Peikang Shelf. Among them, four reach the
so-called Mesozoic Basement, and contain
nannofossils indicating Early Cretaceous A ptian
(or the
Chiastozygus litteraius
Zone and
Pro-
habdolithus abgustus Zone of Thiestein’s 1973)
to Albian in age in the PK-2, PK-3 , MLN-1, and
HP-1 Wells (Huang,
1978).
The overlying
sediments are of the Paleocene Fasciculithus
tympanifonnis Zone (NP
5)
through Discoaster
multiradiatus Zone (NP 9) that have been
recognized from the borehole cores
of
the
WG-1 and THS-1 Wells. The relationship
between the Cretaceous and Paleocene sedi-
ments could be an unconfor mity.
The overlying rocks are widely distributed
Neogene sediments which unconformity cover
the Cretaceous Basement High, or Paleocene
rocks, or some other PreMiocene nanno-
plankton zonation includes the Helicosphaera
kamptneri Zone (approximately equivalent
to NN 2) , the Sphenolithus belemnos Zone
(NN 3 ) , the Helicosphaera ampliaperta Zone
(NN 4), the Middle Miocene
Sphenolifhus
heteromolphus
Zone (NN
5),
and the
Cycli-
cargolithus jloridanus Zone (approximately
equivalent to NN 6). Although th e rock interval
between the upper part
of
the Middle M iocene
and Late Miocene also more or less contain
nannoplankton in some depths, compared to
the abundance in the underlying Early Miocene
sediments, it is extremely rare, or even barren
in nannofossils. Therefore, the age of this
interval is only based on the cores at some
depths. Again, there is
no
deposition
of
this
interval i n some wells. During the Early
Piiocene, the sea trangressed and covered
most of the Peikang Shelf area. Except for
the highest portion of the THS-1 Well where
the Pleistocene
Pseudoemiliania lacunosa
Zone
directly contacts with the Middle Miocene
Sphenolithus heterornolphus Zone, the rest
of the areas of the Peikang Shelf were widely
deposited with the Early Pliocene
Reticulo-
fenestra pseudoumbilica Zone, Late Pliocene
Cyclococcolithus macintyrei Zone, and Pleist-
ocene Pseudoemiliania lacunosa Zone and
Gephyrocapsa oceanica Zone. A fter the deposi-
tion of the Gephyrocapsa oceanica Zone, the
sea quickly regressed from the shelf area and
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348
deposited the alluvial or terrestrial facies
sediments, where no nannofossils have been
recovered.
3. South Taiwan Basin
This basin is situated between the Chiayi
and Pingtung cities. Com pared to northern
Taiwa n, the lithology in this basin is charac ter-
ized by facies change with much more marine
sediments. This coincides well with the results
from various lines of studies that the Peikapng
Shelf has a general tendancy of sloping south-
ward down into the South Taiwan Basin with
the overlying Neogene se dimen ts becoming
relatively thicker and deeper from the north
to the south (Meng et al., 1960 ; Bosum et al.,
1970).
Based on both the geographical and geo-
logical view, the South Taiwan Basin can be
subdivided into three units: the Chiayi area,
the Tainan area, and the Kaohsiung area.
A
total of 21 sections have been studied, six
sections in the Chiayi area, seven in the Tainan
area , and eight in th e Kaohsiung area. The ages
of sediments in this basin varies from Late
Miocene t o Middle Pleistocene.
The Late Miocene sediments which are
moderately common of sandstone, are repre-
sented by the socalled Tangenshan Sandstone,
Mucha Formation, or Chunglun Formation,
exposed in the eastern part of the basin. The
moderately well preserved nannofossil assem-
blages are diversified in this interv al, comp osed
of
Discoaster quinqueramus
Gartner,
Spheno-
lithus abies Deflandre, Reticulogenestra pseudo-
umbilica (Gartner), and Triquetrorhabdulus
rugosus
Bramlette and Wilcoxon, which can
be assigned to the Discoaster quinqueramus
Zone. The continuous sediments above the
Discoaster quinqueramus
Zone are mainly
composed of shale or mudstone, representing
the Early Pliocene Ceratolithus acutus Zone
and Reticulogenestra pseudoumbilica Zone.
The high diversity and good preservation of
the nannoflora in this interval, specially in the
Tainan and Kaohsiung mudstone areas, indicate
open sea and marine conditions during deposi-
tion. The assemblages are com posed o f
Cerato-
lithus acutus Gartner and Bukry,
C.
rugosus
Bukry and Bramlette,
Reticulogenestra pseudo-
umbilica
(Gartner), and
Sphenolithus abies
Deflandre. The Miocene and Pliocene boundary
is placed on the top of the first appearance
datum
of
the
Ceratolithus acutus
Gartner and
Bukry
.
The overlying rocks are mainly comp osed
of sandstone and shale in alteration, bu t poorly
preserved with a lower diversity nannoflora,
including Sphenolithus sp., Discoaster brouw eri
Tan Sin Hok, D. penteradiatus Tan Sin Hock,
and Pseudoemiliania lacunosa (Kamptner).
They can be assigned to the Late Pliocene but
do not allow for more detailed stratigraphic
subdivisions.
The nannoflora flourished again during the
beginhing of the Early Pleistocene. Therefore,
well preserved nannoplankton with high diver-
sity have been recovered from the sediments.
The important species are
Gehyrocapsa oceanica
Kamptner, Gephyrocapsa sp ., and Pseudoemi-
liana lacunosa
(Kamptner). The first appear-
ance datum of Geph yrocapsa Oceania Kamptner
is also used for determ ining the Pliocene and
Pleistocene boundary. The small
Gephyrocapsa
Zone was first introduce d by S. Gartner (1977)
as just below the Jaramilo Event (1.22 M.Y.
0.92 M.Y.). It has also been recognized from
the sediments in the South Taiwan Basin, but
the horizon is within the lower part of the
Brunes Epoch. The datum here is a little
younger than that of Gartner’s suggestion.
This difference probably implies that the small
Gephyrocapsa Zone in Southern Taiwan
is diachronous with the Zone of deep-sea
sediments of Gartner’s suggestion (Chen,
e t
al., 1977) or that there were different deposi-
tional environments (Chi, 19 78).
4. Henchun Peninsula:
The Hengchun Peninsula is located on the
southern tip of the island of Taiwan. Only
three sections have been selected for this stud y:
the Maanshan section, the To ukou section, and
th e Kengting sec tion. The sediments of the first
two sections produce well preserved nanno-
plankton of high diver sity, such as Pseudoemi-
liania Zacunosa
(Kamptner),
Gephyrocapsa
Oceania
Kamptner, and
Discoaster pentara-
diatus Tan Sin Hok, indicating Pliocene to
Pleistocene in age. The sediments of the Keng-
ting section contain fair and moderate diversity
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349
of nannofossils. Not only the ages of the
sediments can be determined, but also the age
differences between the matrix and exotic
blocks can be recognized. Matrix of the Keng-
ting Formation yield associations of the Late
Miocene Discoaster quinqueramus Zone (equi-
valent to
NN 11
of Martin’s zonation), such as
Discoaster quinqueramus Gartner, Reticulo-
fenestra pseudoumbilica (Gartner), and Spheno-
lithus abies Deflandre. The exotic blocks of the
Kengting Formation also produce nannoflora
indicating many different ages. The ages of the
exotic blocks range from the Cretaceous to
the Miocene. The secondarily derived nanno-
fossils include
Sphenolithus heteromorphus
(Deflandre) (NN 3
NN
9
. belemnos
Bram-
lette and Wilcoxon (Late Eocene-Oligocene),
S.
distensus (Martini) ” 3 N p 24), Dictyo-
coccites bisectus (Hay, Mohler, and Wade)
(Eocene-Oligocene), Zygrahablithus bijugatus
(Deflandre) (Oligocene-Eocene), Reticulofenes-
tra umbilica (Levin) (Late Eocene-Early Olig-
ocene), Chiamolithus grandis (Bramlette and
Riedel) (Eocene), Cyclococcolithus f omosus
Kamptner) (Eocene to Early Oligocene), and
watznaueria barnesae (Black) (mesozoic). The
above data indicate that th e Kengting Formation
is a melange or olistostro me dep osited in a
basin near a fault-scarp or nea r the source area.
5 . The Coastal Range
The Coastal Range is located on the eastern
side of th e island of Taiwan. It is characterized
by a number of pyroclastic or tuffaceous agglo-
merates or conglomerates within sediments.
A total of 16 sections have been studied, the
ages ranging from Late Miocene
(NN
9) t o
Early Pleistocene (NN
19).
Although the sediments of the Tuluanshan
Forma tion are m ainly composed of pyroclastic
agglomerates, tuffaceous conglomerates, and
sandstone, the ages can also be determined
from the tuffaceous sandstone in several
sections. The nannofossils include
Discoaster
quinqueramus Gartner,
D.
neohamatus Bukry
and Bramlette, and some other Late Miocene
associations. The nannoplankton becomes
common to abundant in the Pliocene sediments.
Th e nannofossil assemblage is mainly c ompo sed
of Reticulofenestra pseudoumbilica (Gartner),
Sphenolithus abies Deflandre, Ceratolithus
rugosus Bukry and Bramlette, Pseudoemilianic
lacunosa (Kamptner), Gephyrocapsa sp., Dis-
ciaster sulculus Martini and Bramlette, and D.
pentaradiatus Tan Sin Hok. Besides, the Late
Miocene association is also found from the
olistostrome of the Takangkou Formation.
The P leistocene sedime nts are composed of
shale and conglomerates and also contain
moderately preserved nannofossils of high
diversity. The assemblage includes Geohyro-
capsa oceanica Kamptner and Pseudoemiliania
lacunosa (Kamptner). The Lichi fFormation,
exposed in the southern and southwestern
parts of the Coastal Range is proved to be a
melange containing nannofossils of diff erent
ages in matrix and exotic blocks.
CALCAREOUS NANNOPLANKTON DATUMS
AND ZONATIONS
In general, the extremely thick Cenozoic and
some Mesozoic marine sediments exposed on
the southwestern Coastal Plain and eastern
Coastal Range provide rather abundant cal-
careous nannofossils. Based on th e first appear-
ance datum (FAD) and the last appearance
datum (LAD), of socalled “Biostratigraphic
events”, a total of 24 datums and 2 0 biostrati-
graphic zonations have been recognized from
the studied area and proposed. However, in
some sections, marker species occur only
sporadically or are even absent. Therefore,
the zonations are defined relying upon some
othe r diagnostic species.
The calcareous nannoplankton datums are
listed in ascending order as follows:
1) The FAD of Rucinoluthus irregularis
Thiestein, Chiastozygus litteranus
(Gorka),
Braaiudosphaera aficana
Stradner, Parhabdolithus angustus
(Stradner).
(2) The FAD of
Lithastrinus floralis
Stradner
and the LAD of
Micrantholithus obtusus
Stradner.
(3) The FAD
of Fasciculithus ty mp anif om is
Hay and Mohler .
4)
The FAD of Heliolithus kleinpelli Sullivan
5 )
The FAD of Discoaster gem meus Stradner
6 )
The FAD of
Heliolithus riedeli
Bramlette
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3.50
and Sullivan
(7) The FAD of Discoaster multiradiatus
Bramlette an d Riedel
8) The LAD of
Sphenolithus ciperoensis
Bramlette and Wilcoxon, Zygrhablithus
bijugatus
(Deflandre), or
Dictyococcites
bisectus
(Hay, M ohler, and Wade).
(9) The LAD of Sphenolithus distensus
Martini
(10) The FAD of Helicosphaera kamptneri
Hay and Mohler and Discoaster druggii
Bramlette
1 1) The LAD of Triguetrorhabduluscarinatus
Martini
(12) The LAD
ofsphenolithus belemnos
Bram-
lette a nd Wilcoxon
(1 3) The LAD of Helicosphaera ampliaperta
Bramlette and Wilcoxon
(14) The LAD of
Sphenolithus heteromorphus
Deflandre
(1 5) The LAD of
Cyclicargolithus floridanus
(Roth and Hay)
(16) The appearance of Catinaster coalitus
Martini and Bramlette or Discoaster
bollii Martini and B ramlette
(17) The FAD of
Discoaster quinqueramus
Gartner
(18) The FAD
of
Ceratolithus acutus Gartner
and Bukry
19)
The FAD of
Ceratolithus rugosus
Bukry
and B ramlette
(20) The LAD of Reticulogenestra pseudo-
umbilica
(Gartner)
(21) The FAD of Gephyrocapsa oceanica
Kamptner
(22) The first LAD of
Gephyricapsa oceanica
Kamptner
(23) The reappearance datu m of
Gephyrocapsa
oceanica Kamptner
(24) The LAD of
Pseudoemiliania lacunosa
(Kamptner)
Calcareous Nannoplankton Zonations:
Based on th e above datums , together with
detailed insight into the associations, 22 bio-
stratigraphic zones from the sediments of the
studied area are defined in ascending order as
follows:
Lower Greraceous (Aptian):
1
1
Rucinolithus irregularis Zone
Definition
:
Interval from the FAD of
Rucinolithus
irregularis Thierstein to the LAD of Predisco-
sphaera cretacea
(Arkhangelsky).
Occurrence:
This zone is only found from the bore-hole
cores and cuttings of PK-2 (1600-1700m),
PK-3 (2040-2080m), MLN-1 (38 70- 407 0m ),
HP-1 (4000-4050m) by the Chinese Petroleu m
Corporation from the Peikang Shelf.
Common species:
R . irregularis Thierstein, Watzanueria bar-
nasae (Black),
W.
britannica (Stradner), Cru
ciellipsis chiastia
(Worsley),
Braarudosphaera
afn’cana
Stradner,
Nannoconus minutus
Bronni-
mann,
N. truittii
Bronnimann,
Micrantholithus
obtusus Stradner, and Cyclagelosphaera marge-
rali
Noel.
Remarks
:
This zone is equivalent to the
Chiastozygus
litterarius
Zone and the part of the
Porhabdo-
lithus angustus Zone
of
Thierstein’s (1973)
‘zonat ion, or t o most part of the Chiastozygus
litterarius
Zone of Sissingh’s zonation (1977).
A detailed study of this interval has bee n made
by Huang (1978). The base of this zone is
concealed.
Upper Paleocene :
2)
Faciculithus tympaniform is Zone
Definition:
Interbal from the F AD of
F. tympani fom is
Hay and Mohler to the FAD of
Heliolithus
kleinpelli
Sullivan.
Occurrence:
The drilling cuttings of 19 10 m in the THS-1.
Common species:
Fasciculuthus tym pani formis Hay and
Mohler Fasciculithus ulii Perch-Nielsen, Fasci-
culuthus
sp.
Prinsius bisulcus
(Stradner),
Cocco-
lithus pelagicus (Wallich), Toweius craticulus
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351
Hay and Mohler
T. eminens
(Brandette and (5)
Heliolithu s riedeli
Zone
Suilivan),
Zygodiscus signoides
’Bramlette and
Sullivan,
Sphenolithus morifomis
Bronnimann.
Remarks:
This zone is equivalent to the Fa,sciculithus
tympanifomis Zone (NP 5)
of
Martini’s zona-
tion (1971).
A
detailed study of this interval
has been made by T.C. Huang and Chi (1979).
3) Heliolithus kleinpellii Zone
Definition:
Interval from the FAD of Heliolilhus klein-
pellii Sullivan to the FAD Discoaster mohleri
Budry and Percival.
Occurrence :
to 4200m in depths .
Common species:
Zone, plus Heliolithus kleinpellii Sullivan.
Remarks:
This zone is equivalent to the part of the
Heliolithus kleinpellii Aone NP-6) of the
Martini’s zonation (1971). A detaded study
of this interval has been made by T.C. Huang
and W.R. hi (1979) .
The bore-hole cores of WG-1, from 3850m
Those of the Fasciculithus tympanifomis
4) Discoaster moh leri
Zone
Definition:
Interval from the FAD of
Discoaster moh leri
Bukry and Percival to the
FAD
of
Heliolithus
riedeli Bramlette and S ullivan.
Occurrence:
3600m-3850m in depth.
Common species:
Those of the Heliolithus kleinpellii Zone,
plus
Discoaster mohleri
Bukry and Percival.
Remarks
:
This zone is equivalent to a part of the
Discoaster gemm eus
Zone
NP
7)
of
Martini’s
zonation (1971). A detailed study this interval
has been made by T.C. Huang and W.R. Chi
(1979).
Borehole cores of C.P.C. WG-1 Well, from
Definition:
Interval from the FAD of
Heliolithu s riedeli
Bramlette and Sullivan to the FAD of Discoaster
multiradiatus Brandette and R iedel.
Occurrence:
f rom 3500m t o 3300m in depths.
Common species:
Those of the Discoaster mohleri Zone,
plus
Heliolithus nedeli
Bramlette and Sullivan,
Chiasmolithws grandis Bramlette and Riedel,
Fasciculitlzus involutus Bramlette and Sullivan,
F. schaubi Hay an d Mohler in the upper part of
this zon e,
The borehole cores of C.P.C. WG-1 Well
Remarks:
This zone
is
equivalent to a part of the
Heliothus riedeli
Zone, and might go into the
lower part of the Discoaster multiradiatus
zonation (1971). A detailed study of this
interval has been made by T.C. Huang and
W.R. Chi (1979).
6) Sphenolithus distensus Zone
Definition:
Spenolithus distensus (Martini).
Occurrence:
in the Nantou area.
Common species:
Sphenolithus predistentus
Bramlette and
Wilcoxon,
S. distentus
Bramlette and Wilcoxon,
Dicfyococcites bisectus (Hay, Mohler, and
Wade), Cyclicargolithus floridanus (Roth and
Hay),
Sphenolithus morifomis
(Bronnimann
and Stradner).
Remarks:
This interval is equivalent to the Spheno-
lithus distentus zone (NP 24) of Martini zona-
tion (1971), the basal part may down to the
Sphenolithus predistentus zone. A detailed
study of this interval has been made by T.C.
Huang and J.A. Ting (1979).
Interval from the
FAD
to the
LAD
of
The lower part o fth e Shuichangliu Formation
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(7)
Sphenolithus ciperoensis Zone
Definition
:
The LAD of
Sphenolithus distentus
Bram-
let te and Wilcoxon
to
the LAD of
S. ciperoensis
Bramlette and Wilcoxon,
or Dictyococcites
bisectus
(Hay, Mohler, and Wade), or
Zygrha-
blithus bijugatus
Deflandre).
Occurrence:
Interval from the upper part of the Shui-
changliu Formation to the basal part of the
Takeng Formation in the N antou area.
Common species:
Those of the
Sphnolithus distentus
Zone,
except for S.
distentus
Bramlette and Wilcoxon,
the assemblage is the same as plus S.
ciperoensis
Bramlette and Wilcoxon and
Triquetrorhabdulus
carinatus
Martini.
Remarks:
This zone is approximately equivalent to
the
Sphenolithus ciperoensis
Zone
of
Martini’s
zonation (1971). The Tsukeng Formation is
characterized by the occurrence of
Discocyclina
and tuffaceous sediments, was assigned to this
zone, and the blocks containing the Eocene
Discyclina
is
also believed to be derived from
the Peikang Shelf (Chi, 197 9).
8)
Triquetrorhabduluscarinatus Zone
Definition:
Interval from the LAD of
Sphenolithus
ciperoensis
Bramlette and Wilcoxon to the
FAD of
Helicosphaera kamptneri
(Hay and
Mohler), or
Discoaster druggii
Bramlette and
Wilcoxon.
Occurrence:
Within the Lower part of the Takeng Forma-
tion in the Nantou area. May be observed from
the subsurface wells of the Peikang basement
High (Chi, 1980,
in
Chang
et al.,
1980).
Common species:
The lower diversity of
Cyclicargolithus
floridanus
(Roth and Hay).
Coccolithus
pelagicus
(Wallich),
Sphenolithus moriformis
(Bronnimann and Stradner),
Sphenolithus
sp.,
Dictyococcites abisectus
(Muller),
Reticulo-
fenestra sp.,
and
Discoaster
sp.
Remarks:
This
zone
is
roughly equivalent to the
Triquetrorhabdulus carinatus
Zone (NN 1) of
Martini’s zonation (1971). This interval is
equivalent to th e upper part of the Tatungshan
Formation in north Taiwan. The most part of
this zone is rare in nannofossils (Chi, 197 9).
9 ) Helicosphaera hm pt ne ri Zone
Definition:
Interval from the FAD of
Helicosphaera
kamptneri
(Hay and Mohler), or
Discoaster
druggii
Bramlette and Wilcoxon t o the LAD of
Triquetrorhabduluscarinatus
Martini.
Occurrence:
From the upper part of the Takeng Forma-
tion to the basal part of the Shuilikeng Forma-
tion in the Nantou area (Chi, 197 9); the sub-
surface sediments overlying the so-called base-
ment from the Peikang Shelf (Chi, 1980 ,
in
Chang
et
al., 1980); the Piling Shale of the
Miaoli area (Chi and Mei, 1981). (see fig.
3).
Common species:
Triquetrorhabdulus carinatus
Martini,
Cycli-
cargolithus floridanus
(Roth and Hay),
Cocco-
lithus pelagicus
(Wallich),
C. miopelagicus
Bukry
, Distyococcites abisectus
(Muller),
Reti-
culofenestra
sp.,
Sphenolithus dissimilis
Bukry
and Percival,
S
conicus
Bukry,
S
moriformis
(Bronminann and Stradner), S
pacificus
Martini, S.
belemnos
Bramlette and Wilcoxon,
Sphenolithus
sp.,
Discoaster druggii
Bramlette
and Wilcoxon,
Helicosphaera kamptneri
(Hay
and Mohler) or
H. carteri
(Wallich) H.
amplia-
perta
Bramlette and Wilcoxon,
H. intermedia
(Martini),
Discolithina sp., Braarudosphaera
bigelowi
(Gran and Braarud).
Remarks
:
This zone is equivalent to the
Discoaster
druggii
Zone of Bramlette and Wilcoxon’s
zonation (1967), or the
Discoaster druggii
Zone
(NN
2 ) of Martini’s zonation (1971),
or the
D. druggii
Subzone of the
Triquetror-
habdulus cartinatus
Zone of Bukry’s zonation
(1971, 1978).
Helicosphaera kamptneri or
H. carteri
and
D . drug@i
have their first appear-
ance at the base of this zone. This interval
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is equivalent to the Tailiao Fo~mation
in
northern Taiwan: The upper part of the
so-
called Pachangchi Sandstone, and the Molluscan
Limestone in the Peikang Shelf is within this
occurrence:
Within the middle part of the Shuilikeng
Formation of the Nantou area; the subsurface
sediments of the C.P.C. drilling wells (see figure
zone. 3)
10)
Sphenolithus belemnos
Zone
Definition:
Interval from the LAD of Triquetrorhab-
dulus carinatus
Martini to the LAD of
Spheno-
lithus belemnos
Bramlette and Wilcoxon.
Occurrence:
The lower part
of
the Shuilikeng Formation
of
the Nantou area; the subsurface section of
the C.P.C. drilling wells in the Peikang Shelf
(see fig. 3). And also found from the Lushan
Formation near the Liukuei, Kaohsiung area.
Common
species:
Sphenolithus heteromophus
Deflandre, S.
moriformis
(Bronnimann and Stradner),
S.
pacificus
Martini,
Sphenolithus
sp .,
Helicos-
phaera kamptneri
(Hay and Mohler),
H. carteri
(Wallich),
H, intermedia
Martini,
Cyclicargo-
Zithus floridanus
(Roth and Hay),
C)cZococco-
lithina macintyrei
(Bukry and Bramlette),
Coccolithus pelagicus
(Wallich),
C. miopela-
gicus Bukry,
Reticulofenestra
sp
., Discoaster
dejlandrei
Bramlette and Wilcoxon,
D. varia-
bilis
Martini and Bramlette,
D. formosus
Martini and W orsley, and
Discoaster
‘sp.
Remarks:
This zone is equivalent to the
Sphenolithus
heteromolphus
Zone of Bramlette and Wil-
coxon’s zona tion (1967)
or
to the
Sphenolithus
heteromolphus
Zone
(NN 5 )
of Martini’s zona-
tion (1971), or to the S.
heteromoiphus
Zone
of Bukry’s zonation (1973, 1978). This zone
is equivalent to the lower part of the Peiliao
Sandstone in the M iaoli area.
11)
Helicosphaera ampliaperta
Zone:
Definition:
Common
species:
Helicosphaera ampliaperta
Bramlette and
Wilcoxon, H.
kamptneri
(Hay and Mohler).
H. carteri
(Wallich), H
euphratis
Haq,
H.
obliqua
Bramlette and Wilcoxon,
Coccolithus
pelagicus
(Wallich),
C.
miopelagicus
Bukry,
Cyclicargolithus floridanus
(Roth and Hay),
Sphnolithus heteromophus
Deflandre, S.
conicus
Bukry, S.
pacificus
Martini, S. mori-
forms
(Bronnimann and stradner),
Discoaster
deflandrei
Bramlette and Wilcoxon,
D. adaman-
teus
Bramlette and Wilcoxon and
Discoaster
sp.
Remarks:
This zone is equivalent to the interval from
the upper part of the Peiliao Sandstone to
the lower part of the Talu Shale in Northern
Taiwan. The socalled
Orbitoid
Limestone is
within the upper part of this zone.
12)
Sphenolithus heteromorphus
Zone
Definition:
Interval from the LAD of
Helicosphaera
ampliaperta
Bramlettea and Wilcoxon to the
LAD
of Sphenolithus heteromolphus
Deflandre.
Occurrence:
The middle part of the Shuilikeng Forma-
tion of the Nantou area; the subsurface sedi-
ments
of
the C.P.C. drilling wells of the Peikang
Shelf (see fig.
3).
Common
species:
Sphenolithus heteromophus
Deflandre, S.
morifomis
(Bronnimann and Stradner), S.
paci-
ficus
Martini,
Sphenolithus
sp.,
Helicosphaera
kamptneri
(Hay and Mohler),
Cyclococcoli-
thina macintyrei
(Bukry and Bramlette), Cocco-
lithus pelagicus
(Wallich),
C miopelagicus
Bukry,
Reticulo fenestra sv. Discoaster deflan-
Interval from the LAD of
Sphenolithus
belemnos
Bramlette and Wilcoxon t o the LAD
of
Helicosphaera ampliaperta
Bramlette and
Wilcoxon. and
Discoaster
sp.
drei
-Bramlette and Wilcoxon,
D. variabilis
Martini and Bramlette,
D. exilis
Martini and
Bramlette,
D. formosus
Martini and Worsley,
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Remarks:
This zone is equivalent to the interval from
the upper part of the Talu Shale to the basal
part of the Kuanyinshan Sandstone in Northern
Taiwan.
13) Cyclicargolithus loridanus Zone
Definition
Interval from the LAD of
Sphenolithus
heteromophus
Deflandre to the LAD of
Qclicargolithus floridanus
(Roth and Hay).
Occurrence:
Within the lower upper part of the Shui-
changliu Formation of the Nantou area; the
subsurface borehole sediment of the Peikang
Shelf.
Common species:
Cyclicargolithus floridanus
(Roth and Hay),
Sphenolithus pacijicus
Martini,
S. rnorifonnis
fonnis (Bronnimann and Stradner), Helicos-
phaera kamptneri (Hay and Mohler), Q c l o -
coccolithina macintyrei
(Bukry and Bramlette),
Cy. leptopora
(Murray and Blackman),
Reti-
culofenestra sp., Reticulofenestra of R. pseudo-
umbilica (Gartner), Coccolifhus pelagicus
(Wallich), Discoaster exilis Martini and Bram-
lette,
D. variabilis
Martini and Bramlette,
Discoaster sp. and Triquetrorhabdulus rugosus
Bramlette and Wilcoxon.
Remarks:
This zone is equivalent to the part of the
Discoaster exilis
Zone
of
Martini’s zonation
(1971), or to the Coccolithus miopelagicus
Subzone of the Discoaster exilis Zone of the
Bukry’s zonation (1978). The top of this zone
is within the middle part of the Kuanyinshan
Sandstone Member of the Nankang Formation
in northern Taiwan.
14)
Discoaster variabilis Zone
Definition:
Interval from the LAD of Cyclicargolithus
floridanus
(Roth and Hay) to the FAD of
Discoaster quinqueram us
Gartner.
Occurrence
:
Within the upper part of the Shuilikeng
Formation of the Nantou area; within the
lower part of the Nanchuang Formation,
eastern flank of th e Chunglun anticline, 1650m
depth pf CL-1 Well in th e Chiayi area, and th e
Shanmin Shale of the Hunghuatzu section,
Kaohsiung area.
Common species:
Reticulofenestra pseudoumbilica
(Gartner),
Reticulofenestra sp ., Dictyococcites hesslandii
(Haq), D. minutus (Haq), Coccolithus pelagicus
(Wallich), C. miopelagicus Bukry
,
Helicosphaera
kamptneri Sphenolithus morifomis (Bronni-
mann and Stradner),
S.abies
DeflandreJpheno-
lithus sp., Helicosphaera kamptneri (Hay
and Mohler),
Cyclococcolithina macintyrei
(Bukry and Bramlette),
Coronocyclus nitescens
(Kamptner), Discoaster of D. kuglen Martini
and Bramlette, D. bollii Martini and Bramlette,
D. varialilis Martini and Bramlette, D. varialilis
Martini and Bramlette,
D. exilis
Martini and
Bramlette,
Discoaster
sp., and
Catinaster
sp.
Remarks:
Owing to the lower diversity, or lack of key
markers such as Discoaster kugleri, D. ham atus,
and Catinaster coalitus in this area, only the
LAD of
Cyclicargolithus floridanus
can be used
for the base, and only the FAD of Discoaster
quinqueramus, or Ceratolithus sp. can be used
for the to p to define this zone.
This zone is equivalent to the interval from
the base of Zone NN 7 to the top of zone NN
10 of Martini’s zonation (1971). This zone is
also
equivalent to the interval from the upper
part of the Discoaster exilis Zone to the to p of
the D. neohamatus Zone of Bukry’s zonation
(1978).
D. bollii, D. kulgeri
and
Catinaster
coalithus
have their first appearance (in lower
diversity), near the base of this zone.
15) Discoaster quinqueramus
Zone
Definition:
Interval from the FAD of
Discoaster quin-
queramus Gartner to the FAD of Ceratolithus
acuius Gartner and Bukry.
Occurrence:
The lower part of the Mucha Formation or
the Tangenshan Sandstone in the Tainan area;
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the lower part of the Wushan Formation in
the Kaohsiung area; within the middle part of
the Chunglun Formation in the C'hiayi area;
the lower part of the Tangenshan Sandstone
of the Hunghuatzu section; the upper most
part of the Shuilikeng Formation in the N antou
area; the Kengting Formation in the H engchung
area; the upper part of the Tuluanslian Forma-
tion of the Coastal Range, eastern Taiwan; and
some subsurface sections in the Peikang Shelf.
Common species:
Large form of Reticulofenestra pseudoum-
bilica (Gartner), Sphenolithus abies Deflandre,
Sphenolithus
sp. ,
Cyclococcolithina macintyrei
(Bukry and Bramlette), Cy.
leptopora
(Murray
and Blackman), Helicosphaera kam ptnen (Hay
and Mohler), Coccolithus pelagicus (Wallich),
Discoaster brouweri Tan Sin Hok, Discolithina
multipora, Discoaster quinqueramus
Gartner,
D. variabilis Martini and Bramlette, Discoaster
sulculus
Martini and Bramlette,
D. chanllengeri
Bramlette and Riedel,
Dictyococcites mininus
(Haq), Amaurolithus tricorniculatus (Gartner).
Remarks:
According to Gartner (1969) and Martini
(1970), the definition
of
the
D. quinqueramus
zone was based on the FAD and last appearance
(LAD) of the D. quinqueramus. The upper
limit
of
the marker species of this zone is
only incompletely known, but it seems to be
restricted to Upper Miocene arid possible
Lowermost Pliocene sediments (GaItner, 1969,
p. 598). Haq and Berggren
(1
978) also reported
that the species occurs in the EaIly Pliocene
and does not disappear until the end of the
Early Pliocene (NN 15) in core 67 of the Rio
Grande Rise in the Atlantic Ocean. They also
maintained that the anolamous LAD
of D.
quinqueramus cannot be explained by rework-
ing alone, and must sought in either the time
transgressive nature of this event, or in differing
taxonomic concepts (Haq and FAD of D.
quinqueramus
for the base of this zone is
reliable, the LAD of this species
IS
uncertain
so
far.
Although the distribution of D. quinquera-
rnus
is dispersed in the above sections, because
it
persists in this interval and no
A . amplificus
or C. acurus has been foun d, he writer proposed
tha t this interval is equivalent the upper part of
the
D.
quinqueramus Zone and lower part of
the C
tricorniculatus
Zone of Gartner's (1 969)
or Martini's (1970), or Bukry's (1971), or the
upper part of the D. quinqueramus zone and
C. acutus
zone of Haq's (1978). This zone can
also be correlated with the lower part of the
Kuantaoshan Sandstone of the Chuhuangkeng
section.
16) Ceratolithus acutus Zone
Definition:
Interval from the FAD of
Ceratolithus
acutus Gartner and BiJkry to the FAD of
Ceratolithus
rugosus Bukry and Bramlette.
Occurrence:
Within the middle part of the Mucha Form a-
tion , or spands the interval from the upper part
of the Tangenshan Sandstone to the lower part
of the Yunshuikeng Shale in the Tainan area;
the interval from the upper part of the Wushan
Formation to the m idd e part of the Kaitzuliao
Shale in the Kaohsiung area; the interval from
the upper part Kaohsiung area; the interval
from the upper part of the Chunglun Forma-
tion t o the basal part of th e Niaotsui Formation
in the Chiayi area; and the lower part
of
the
Takangkou Formation in the Coastal Range
eastern Taiwan.
Common species:
Sphenolithus abies Deflandre, Sphenolithus
sp., Cyclococcolithina macintyrei Bukry and
Bramle t e, Helicosphaera kamp tneri (Hay
and Mohler), Reticulofenestra pseudoumbilica
(Gartner), Coccolithus pelagicus (Wallich),
Discolithina
sp.,
Discoaster brouwen
Tan Sin
Hok, D. variabilis Martini and Bramlette, D.
suducalus
Martini and Bramlette, Discoaster
of D. pentaradiatus Tan Sin Hok, Dictyo-
coccites mininus
(Haq),
Dictyococcites heesi-
landii (Haq), Amatolithus amplificus (Bukry
and Percival), A .
primus
(Bukry and Percival),
A . delicatus
Gartner and Bukry, A .
tricornicu-
Eatus
(Gartner),
Ceratolithusacutus
Gartner and
Bukry.
Remarks
:
According to Bukry (1971), his
C. tricorni-
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culus Zone can be subdivided into the Trique-
trorhabdulus rugosus subzone, A. amplificus
subzone, and C rugosus subzone, the late
(1973), he took the
Ceratolithus acutus
Sub-
zone is based on the interval between the
FAD of C. acutus and the FAD of C.
rugosus.
(Bukry, 1973). This subzone is equivalent to
the interval between the basal part of
NN
12
and the top of
NN
13 of Martini’s.
Due to the sparse distribution
of
the
acutus
in some th e base of this zone is difficult
to distinguish from the D. quinqueramus
Zone. The writer would rather distinguish
them based on th e different assemblages. In
experience, the
C. acutus
Zone contains a
higher frequency of the
Amaurolithus
or
Ceratolithus species than the D. quinqueramus
Zone. In other words, it is easier to find the
species of
A. delicatus A. primus A . tricomi-
cus A. amplificus C. acutus
and other
Cera-
tolithus species in this zone than in the D.
quinqueramus
Zone. Furthermore,
D. quin-
queramus
seems distinct within this zone in the
studied area.
This zone can be correlated with the upper
part of Zone
NN
12 of Martini’s, and the C.
acutus subzone
of
the C tricorniculatus Zone
of
Bukry’s and can also be correlated to the
upper part of the Kuantaoshan Sandstone and
the lowermost part of the Shihliufen Shale of
the Chuhuangkeng section, Northern Taiwan.
17) Reticulofenestra pseudoumbilicaZone
Definition:
Interval from the FAD of
Certolithus
rugosus
Bukry and Bramlette to the LAD of
Reticulofenestra pseudoumbilica (Gartner).
Occurrence:
The interval from the upper part of the
Yenshuikeng Shale to the basal part
of
the
Yunshuichi Formation, or the Chutouchi
Formation, or within the lower part of the
Lower Gutingkeng Formation in the Tainan
area; the interval from the upper part of the
Kaitzuliao Shale to the top of the Nanshihlun
Sandstone in the Kaohsiung area; the interval
from the lower part of the Niaotsui Formation
to the upper part
of
the Yunshuichi Formation
in the Chiayi area; and within the middle part
of the Takangkou Formation in the Coastal
Range, eastern Taiwan.
Common species:
Sphenolithus abies Deflandre, Sphenolithus
sp.,
S moriforms
(Bronnimann and Stradner),
Ceratolithus rugosus Bukry and Bramlette,
Amaurolithus tricomiculatus
(Gartner),
Cera-
tolithus
sp.,
Discoaster surculus
Martini and
Bramlette,
D. pentaradiatus
Tan Sin Hok,
D.
variabilis Martini and Bramlette, D. challengeri
Bramlette and Tiedel,
D. brouweri
Tan Sin Hok,
Reticulofenestra pseudoumbilica
(Gartner),
Re ticulo enestra s
p
. Dictyococcites h essilandii
(Haq), D. mininus (Haq), Cyclococcolithina
leptopora (Murray and Blackman), 0 acin-
tyrei
(Bukry and Mohler),
H. selli
Bukry and
Bramlette,
Discolith na japonica
(Takayama),
Discolithina sp ., Braarudosphaera begilowi
(Gran and Braarud) and derived
fossils: Cycli-
cargolithus floridanus
(Roth and H ay),
Spheno-
lithus hetermorphus
(Deflandre).
Remarks:
According to Gartner (1969) and Martini
(1970) the lower limit of
C. rugosus
Zone (NN
13) is based on the FAD of C
rugosus.
Althougg
its distribution is sporadic, this e vent is reliable
in Southern Taiwan. The upper limit of NN 13
is based on the FAD of
D. asymmetricus
but
it seems unreliable in this area, because the
FAD
of
the species seems to appear earlier than
NN 14 of M artini’s. The same phenom enon
has been reported from the Chuhuangkeng
section (T.C. Huang, 197 6; Chi, 1978 , un-
published data).
The upper limit of
NN
14 of Martini’s is
based on the LAD of
A . tricomiculatus.
This
event seems unreliable in Taiwan too. It is
because this species is too rare in distribution
to be taken as a reliable indicator. The only
event that can be used is the LAD of
R. pseudo-
umbilica.
This zone is equivalent to NN 13
-NN 15
(Early Pliocene) o f Martini’s standa rd zonation.
18) Cyclococcolithina rnacintyreiZone
Definition:
Interval from the LAD of
Reticulofenestra
pseudoumbilica
(Gartner) to the FAD of
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Gephyrocapsa oceanica
Kamptner.
Occurrence :
The interval from the upper part of the
Yunshuichi Formation to the lower part of
the Liuchungchi Formation in the Chiayi area
and Tainan area; Interval from the upper part
of the Chutouchi Formation to the lower part
of the Peiliao Shale, within the middle part
of the Lower Gutingkeng Formation in the
Tainan area; the lower part of the Maanshan
Formation in the Hengchun Peninsula; the
upper part
of
the Takangkou Formation of
Eastern Hsiukuluanchi section in the Coastal
Range, Eastern Taiwan; and thie subsurface
section
of
the Peikang Shelf.
Common species:
Pseudoemiliania lacunosa (Kamptner).
Gephyrocapsa sp. (Small type), Cyclococcoli-
thina leptopora
(Murray and Blackman),
Cy.
macintyrei
(Bukry and Bramleile),
Helico-
sphaera kamptneri
(Hay and Mohiler),
H. selli
Bukry ,
Coccolithus pelagicus
(Wellich),
Emi-
liania ovata
Bukry,
Discolithina
sp., and derived
fossils Cyclicargolithus floridanus (Roth and
Hay), Sphenolithus hetermorphus Deflandre.
Remarks:
This zone is tentatively correlated with
Zones
NN
16 t o NN 18 (Late Pliocene)
of
Martini's zonation. According to Gartner
(1969) and Martini, the base of
D. surculus
Zone (NN 16) is based on LAD
of
R. pseudo-
umbilica. The top boundaries of NN 16 and
NN
17 are based on the LAD
of
D. sulculus
and
D.
pentaradiatus respectively. Because
both of the above markers are sporadic in
distribution in this area, the boundaries of the
three zones are ambiguous. Therefore, the
writer combined the three zones into the
Cyclococcolithina macintyrei Zone. This zone
can also be correlated with the lower part
of the Cholan Formation of the Chuhuangkeng
section.
(1
9)
Pseudoemiliania lacunosa Zone
The definition of this zone is between the
FAD
of
Gephyrocapsa oceanica Kamptner and
LAD of
Pseudoemiliania lacunosa
[(Kamptner).
This zone spans a long interval, it can be sub-
divided into three subzones as follows:
A .
Coccolithus doronicoides Subzone
Definition:
Interval from the FAD of Gephyrocapsa
oceanica Kamptner to the first rapid decrease
or absence of Gephyrocapsa oceanica Kamptner.
Occurrence:
The upper part of the Liuchungchi Forma-
tion in the Chiayi area and Tainan area; the
upper part of the Peiliao Shale or within the
upper middle part of the Gutingkeng Forma-
tion in the Tainan area; the Lingkou Formation
in the Kaohsiung area; the upper part of the
Maanshan Marl in the Hengchun Peninsula;
the lower part of the Takangkou Formation
in the Western Hsiukuluanchi section in the
Coastal Range, Eastern Taiwan, and the sub-
surface of the Peikang Shelf.
Common species:
Gephyrocapsa oceanica
Kamptner,
Gephyro-
capsa sp., (Small type), Pseudoemiliania lacu-
nosa (Kamptner), Cyclococcolithina leptopora
(Murray and Blackman), Cy. macintyrei (Bukry
and Bramlette), Cy. macintyrei (Bukry and
Bramlette),
Helicosphaera selli
(Bukry),
H.
kamptneri
(Hay and Mohler),
Emiliania ovata
Bukry ,
Cocc olithus pelagicus
(Wallich),
Spheno-
lithus sp., and derived fossils: Cyclicargolithus
floridanus (Roth and Hay), Sphenolithus
hetermorphus Deflandre, Reticulofenestra
pseudoumbilica
(Gartner).
Remarks:
According to Gartner (1977), the Pseudo-
emiliania lacunosa
Zone (NN 19 of Martini's)
can be subdivided into four zones, of which
the lowermost one is the Cy. macintyrei Zone
which was defined as the interval between
the LAD of D. brouweri and the LAD of Cy.
macintyrei
and the LAD
of H. sellii
(Gartner,
1977). However, because both
Cy. macintyrei
and
H. sellii
are sporadic in occurrence, both
these biostratigraphic events are unreliable as
markers in study area. Therefore, the only
feasible way is to use the LAD of F. oceanica
as the lower limit marker of this subzone, and
the LAD of H. sellii and the great decrease in
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abundance of
G. oceanica
for the upper limit
marker.
B.
Small
Gephyrocapsa
Subzone
Definition:
The interval from the first rapid decrease or
absence of Gephyrocapsa oceanica Kamptner
to its abundant reappearance. Another charac-
teristic is that the small
Gephyrocapsa
spp.,
dominates in this zone.
Occurrence :
Within the lower part of the Kanhsialiao
Formation in the Chiayi and Tainan area; the
lower upper part of the Lower Gutingkeng
Form ation in the T ainan are a; the interval
from the top part of the Takangkou Formation
to the basal part of the Chimei Formation in
the Coastal Range, EAstern Taiwan.
Comm on species:
Gephyrocapsa spp. (Small type), Pseudo-
emiliania lacunosa (Kamptner), Coccolithus
doronicoides Black and Barnes,
C.
pelagicus
(Wallich), Helicosphaera kamptneri (Hay and
Mohler), Cyclococcolithina leptopore (Murray
and Blackman), and derived fossil:
Cyclicargo-
lithus floridanus (Roth and Mohler).
Remarks:
According to Gartner, the small
Gephyro-
capsa Zone is defined as the interval from the
highest occurrence of H. sellii to the highest
level of dominantly small Gephyrocapsa
(Gartner, 1977). On account of the reworking
problem, both the Cy. macintyrei datum and
the
H. sellii
datum are unreliable in this area.
Therefore, using the LAD of the G. oceanica
instead of the H. sellii datum for the lower
limit of the Small Gephyrocapsa subzone is
more useful in this area. This subzone can
also
be recognized in the upper part of the Lower
Gutingkeng Formation of the Chishan section
which is located south of the Kuan miao section
(Chen
et al.,
1977).
C. Pseudoemiliania lacunosa subzone
Definition
:
The interval from the reappearance of
Gephyrocapsa oceanica
Kamptner to the LAD
of Pseudoemiliania lacunosa (Kamptner).
Occurrence:
The interval from the upper part
of the
Kanhsialiao Formation to the basal part of the
Liushuang Formation in the Chayi and Tainan
area; the interval from the upper part of the
Lower Gutingkeng Formation to the basal part
of the Liushuang Formation; within the Chimei
Formation in the Coastal Range, Eastern
Taiwan.
Comm on species:
Gephyrocapsa oceanica Kamptner, Gephy-
rocapsa spp. (Small type), Pseudoemiliania
lacunosa (Kamptner), Coccolithus productus
(Kamptner),
C pelagikus
(Wallich),
Helicos-
phaera kamptneri (Hay and Mohler), Emiliania
ovata Bukry, Thoracosphaera saxia Stradner,
Cycloccolithina leptopora Deflandre, Cycli-
cargolithus floridanus (Roth and Hay), Reti-
culo
enestra pseudoumbilica (Gartner).
Remarks:
The interval of this subzone is much longer
than of the other zones of the Pleistocene. It
can be correlated with the P. lacunosa zone of
Gartner's (1977), which is equivalent
to
the
interval from the highest level of dominantly
small
Gephyrocapsa
to the highest occurrence
of
P.
lacunosa.
20)
Gephyrocapsa oceanica
Zone
Definition:
Above the interval of the LAD of Pseudo-
emiliania lacunosa (Kamptner). The to p of this
zone is unknow n.
Occurrence:
Within the Liushuang Formation in the
Chiayi and Tainan area and the subsurface
sections of the Peikang Shelf.
Comm on species:
Gephyrocapsa oceanica Kamptner, Gephyro-
capsa
spp. (Small type),
Coccolithus productus
Helicophaera kamptneri (Hay and Mohler),
CoccoZithus pelagicus (Wallich), and derived
fossils:
Sphenolithus abies
Deflandre,
Reticulo-
fenestra pseudoumbilica (Gartner), Cyclicargo-
lithus gloridanus
(Roth and Mohler).
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Remarks:
The zone is equivalent t o the IGephyrocapsa
oceanica (NN 20) Zone of Martini's (1970) a nd
the G. oceanica Gartner's (11969, 1977).
According to them, this zone is defined as
between the LAD of P.
lacunosa
and the FAD
of
Emiliania huxleyi,
unfortunately, the upper
part of this zone is concealed in Taiwan.
STRATIGRAPHIC CORRELATIONS
Biostratigraphic correlation in central and
southwestern Taiwan has been established
based on Foraminifera study by L.S. Chang
(1967, 1975), T. Oinomikado and T.Y. Huang
(1957) , Huang (1963 ,1967 ,1971 ,1975 ,1977 ,
1978); and based on nannofossils by T.C.
Huang (19 78, 1 980 ,197 9), Chen
et al.,
(1977),
and Chi, ( l97 8 ,1 979 ,19 80 ,1 981 a, 1981b).
Based on biostratigraphic events not only
th e detailed stratigraphic zones can be correlated
with one another among the sections in the
basins, but also stratigraphic correlations can
be made from the central part to southern part
of
western Taiwan. F urthe rmo re. the relations
of
the s edimen ts of the Coastal Range, ofeaster n
Taiwan, and of southwestern Taiwan can also
be understood.
As presente d in Figure 3 , the writer selected
one or two type sections from each basin to
show the lithology, and the stratigraphic
correlations among the basins and areas. For
further details of the nannobiostratigraphic
work, refer to other writer's papers (1978,
l 9 7 9 , 1 9 8 0 , 1 9 8 1 a , 1 9 8 1 b) .
Triquetrorhabdulus carinatus Zone (Zone NN
1) by Martini (1971), which is a little above the
LAD of
S.
ciperoensis Bramlette and Wilcoxon;
or on the top of the
Cyclicargolithus abisectus
Subzone (CN la) of the T.
curinatus
Zone (CN
1) based on the end of acme of C. abisectus
(Muller) by Bukry (1978), and a Okada and
Bukry (1980). The boundary is approximately
coeval with the NP 25/NN 1 boundary of
Martini's zonations as discussed by Couvering
(1977). However, the last appearances of
Sphenolithus ciperoensis Bramlette and
Wilcoxon,
Dictycoccites bisectus
(Roth and
Mohler), and
Zygrhablithus bijiagatus
(Deflan-
dre) are approximately at the same level within
the basal part of the Takeng Formation in the
Nantou area. Therefore the datum is used for
determining the Oligocene/Miocene boundary.
2) Miocene/Pliocene Boundary
The problems associated with the deter-
mination of the position of the Miocene and
Pliocene boundary based on planktonic micro-
fossils have had a long and complex history
spanning more than the last decade (Beggren
and Van Couvering, 1974 ). Based on calcareous
nannoplan ktons, various boundaries have been
proposed by different authors. Some authors
placed the boundary within the
Certolithus
rugosus Zone (Bukry, 1971 , 197 2; Martini and
Worsley, 1 970 , Martini, 1 971) ; some placed
it on the top of the
C.
rugosus Zone (Bukry,
1972 ; Gartner, 1973); and some placed it on
the top of the
Ceratolithus acutus
Subzone of
the
Ceratolithus tricomiculus
Zone based on
I
BOUNDARIES
(Martini, 1971). For uractical uuruoses, the
1)
Oligocene/Miocene Boundary
The Oligocene/Miocene boundary is only
recovered from the basal part of the Takeng
Formation of the Takeng, Tsukeng, and Pei-
kangchi sections in the Nantou area, central
Miocene/Pliocene bounhary was placed
on
the
Ceratolithus acutus Subzone of Ceratolithus
triconiculatus Zone of Bukry's (1973, 1978)
based on the FAD of
Ceratolithus acutus
Gartner and Bukry.
Wesyern Taiwan. The boun dary is based on the In s outhe rn Taiwa n, th e Miocene/Pliocene
last appearance of Spheizolithus cipertoensis boundary can be determined based on the FAD
Bramlette and Wilcoxon, Zygrhablithus biju- of Ceratolithus acutus Gartner and Bukry . The
gatus
(Deflandred), and
Dictyococcites bisectus
boun dary is suggested within the middle pa rt of
(Hay, Mohler, and Wade).
The
Oligocene/ the Tangenshan Sandsto ne or within the middle
Miocene boun dary was definedl within the part
of
the Mucha Formation in the Tainan
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area; within the upper part of the Wushan
Form ation in the Kaohsiung area; in the basal
part of the Takangkou Formation in the Coast
Range, eastern Taiwan. The Miocene/Pliocene
boundary defined in southwestern based
on calcareous nannoplankton approximately
coincides with the boundary based on plank-
tonic Foraminifera study by T.Y. Huang
(1977). The M/P bound ary is placed on the
base of the Shihliufen Shale of the Kuechulin
Formation in northern Taiwan.
3) Pliocene/Pleistocene Boundary
The Pliocene/Pleistocene boundary, as the
Miocene/Pliocene bound ary, has had a long and
complex history during more than the last
decade. In planktonic microfossil study, some
of the authors suggested the P/P boundary
based on the extinction of the Genus
Dis-
coaster
and
Globigeriodes quadrilobatus fistu-
losus,
and the first abundant occurrence of
Globorotalia truncatulinoides
(Ericson
et al.,
19 63) ; some of the authors suggested its
boundary based on the LAD of Discoaster
brouweri Tan Sin Hok (A ker, 196 5; Wray
and Ellis, 19 65 ; Berggren
et al.,
1967; Hay
et al.,
196 9; Takayama, 19 69); some of the
authors suggested the FAD of Gephyrocapsa
oceanica
Kamptner for the P/P boundary
(Martini, 1 971 ; Bukry, 197 1; Haq, et al.,
1977 ; Gartner
,
1977
;
Th e boundary can also be proposed based on
the FAD of Gephyrocapsa oceanica Kamptner
in central and southwestern Taiwan. In other
words, the Pliocene and Pleistocene boundary
can be suggested within the middle part of the
Liuchungchi Formation in the Chiayi area and
several sections of the Tainan area; within the
lower part
of
the Lower Gutingkeng Formation
or within the middle part of the Peiliao Shale
in the Tainan area; within the lower part of
Takangkou Formation of the Chengkung
section in the Coastal Range, eastern Taiwan.
The Plio-Pleistocene bound ary is placed
within the middle part of the Cholan Forma-
tion in northern Taiwan.
REMARKS ON GEOHISTORY, PALEO-
ENVIRONMENT, AND TECTONIC SIGNI-
FICANCE
Although detailed work on the geohistory,
paleoecology and tectonic movement of the
study area, has not been systematically carried
out, a little can be learned from the studies on
biostratigraphy, lithology paleoenvironment,
sedimentation rate, fossil preservation, fossil
diversity, and secondary fossils of the sediments.
Based on the biostratigraphic study, at least
three stratigraphic gaps can be recognized from
the sediments of the Early Cretaceous or Late
Paleocene and Early Miocene, of the Miocene
and Late Miocene, and of the end of Early
Pleistocene. The oldest gap
is
between the E arly
Cretaceous and the Early Miocene sediments.
This gap can only be recognized in the Peikang
Shelf area, where the Early Cretaceous Aptian
sediments are overlain by the Early Miocene
”
1
NN
2)
Pachanchi sandstone in the
PK-2, PK-3, MLN-1 and HP-1 Wells. Never-
theless in the Taishi and Wangkung areas
the underlying sediments of the Miocene
Pachangchi Sandstone are the Late Paleocene
(NN
5 NP
10) rock s. The sediments between
the Pachangch Sandstone and the Cretaceous
or Paleocene sediments are tuffaceous material.
The biostratigraphic data indicate that the
Early Cretaceous Sea came from the so uth to
cover the Peikang area up to the north or
northeast, and deposited the Cretaceous and
Paleocene sediments, and a little of Eocene
sediments. Until the Early to Late Oligocene,
the sea extended to the Nantou area and
deposited the Paileng sandstone and the Shui-
changliu Formation. In the meantime, the
Peikang area was lifted and associated with
the intense vo lcanic activity to provide material
to the Nantou area. The intense volcanic activity
on the Peikang Shelf, and in the Nantou area
as well, can be proved by the sediments rich in
tuffaceous material in the Tsukeng Formation
of the Nantou area and in the subsurface
section of the Peikang area. The Oligocene
reddish tuffaceous shale of the Tuskeng Forma-
tion contains Late Cretaceous, Paleocene,
and quite common Eocene secondary nanno-
plankton fossils. In contrast, Late Cretaceous
and Eocene sediments are lacking in most
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parts of the Peikang Shelf. This contrast might
indicate that the Late Cretaceous, Paleocene
(Except for th e Taihsi and Wangkung areas),
and Eocene sediments in the Peikang area were
eroded away during the L ate Oligocene, or that
during the Late Oligocene, the Peikang area or
the adjacent areas are regarded
as
a part of the
source of sediments of the lower part of the
Tsukeng Formation during its deposition in the
Nantou area (Chi, 1979). The unconformity
below the Miocene sediments might be cor-
related with the Puli Orogeny of Chang’s
(Chang, 1955).
During the beginning of the Miocene, the
transgressive sea great in scale covered the
whole of the Peikang and Nantou areas and
deposited the transgressive basal sand, the
Pachangchi Sandstone, in most pairts of the
two areas. The environment of the Pachangchi
Sandstone can also be proved b y its (containing
quite a few of shallow water and nearshore
species, such as
Discolithina
and Bruudos-
phaera bigelowi,
which agrees well with the
lithology of the sandstone. The Miocene sea
covered the area until the Late M iddle Miocene
and deposited the continuous sequence of
sediments from the Early Miocene to the
Middle Miocene (NN 1 NN
8).
During the
end of the Middle Miocene, the sea regressed
and deposited the NN 8/9 marine sediments
in the Nantou area and the outer parts of
the Peikang Shelf. Therefore no NN 8/ NN 9
sediment has been found from the center part
of the Peikang area. Until the Late Miocene,
transgressive sea small in scale covered parts
of the Peikang Shelf and the Nantou areas
again, the covered area increasing to younger
age, and deposited rather shallow and Warner
Late Miocene and Pliocene sediments in most
parts of the N antou area and the Peikang Shelf,
except for the Taihsi area where deposition
did not occur until the Early Pleistocene. This
is the second unconfirmity in th e Peikang Shelf,
but its extent depended on the areas. In other
words, the stratigraphic gap becomes greater
towards the center part of the basement high,
or Taihsi, Peikang and Wangkung areas. The
Late Miocene Sea also covered the whole of
the southwestern Taiwan area and (deposited
the succession of sediments of the interval
from the Late Miocene to the Pliocene. Until
the Early Pleistocene, the large in scale Pleist-
ocene Sea not only covered the Nantou and
Peikang areas, but also the southern part
including the Chiayi, Tainan, Kaohsiung,
and H engchuan areas.
Comparing the paleoenvironment of the
central part and the southern part of western
Taiwan, it seems to show that the paleodepth
was getting rather deeper from north
to
south
based
on
the higher diversity of planktonic
microfossils. Such data also agree well with the
geophysical data, which show tha t t he sea over
the continental shelf was shallow to the north
while water deepened to the south into the
south China Sea. The magnetic contours also
show the gentle gradients and general smooth-
ness indicative of a deep magnetic basement
(see W. Bosum,
e t al.,
1970).
At the end of the Early Pleistocene, tectonic
movement large in scale occurred in most parts
of the island of Taiwan and deposited the
youngest sediments, such as gravel, conglo-
merates, and non-marine loose sand, in the
central and southern part of western Taiwan.
This movement is called the Penglai Island
Orogeny by Chang (1955).
The geology of the Coastal Range is quite
different from that of western Taiwan. It is
characterized by containing island arc material,
conglomerates, marine sediments, and many
different ages of the sedimentary and mafic
exotic blocks. These materials provide the
data for study on the stratigraphic record of
interactions between the Philippine Sea and
Asia Plates.
The end of abundant island arc volcanism
in the Coastal Range is recorded by the Late
Miocene (NN
11)
Tuluanshan Forma tion, but
local island arc volcanism continued up into
the Pliocene and Early Pleistocene
(NN
13
NN 19) as evidenced by tuffs and tuffaceous
sandstones interbedded with mudstones of
the Takangkou Formation in the Coast Range,
eastern Taiwan.
The Neogene paleoenvironment of the
eastern Coastal Range is quite different from
that
of
western Taiwan based on Foraminifera
(see J.C. Ingle, 1975). The result shows that
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the paleodepth of the sediments in the Coastal
Range is about 2000 meters, much deeper than
that in western Taiwan about 500
00
meters.
With the Middle Pliocene (NN 15), there is a
marked increase in the rate of clastic deposition
increasing from less than 500 m/M.Y. to as
much as 11,0 00 m/M.Y. in Early Pleistocene,
which agrees with the influx of sediments from
the protoCen tra1 Mountains source to the
west, recording the beginning of collision
(ab out 4 M.Y.) of the Philippines Sea Plate
with the Chinese Continental Margin (Chi,
e t al., 1981). The stratigraphical record of
the plate interactions in the Coast Range also
agrees with the record of uplift tectonic move-
ment in western Taiwan. In western Taiwan,
the secondary fossils increased in abunda nce
from the Late Pliocene, and the rates of sedi-
mentation was also increased rapidly during
the rates of sedimentation was also increased
rapidly during the Early Pleistocene (Chen,
e t
al.,
1977). Such data show that tectonic
movements played an important role from the
Post-Late Pliocene, especially in the Pleistocene.
This agrees well with the age record of the
collision between the Luzon Island Arc and the
Chinese Continental Margin in the Coastal
Rang e, eastern Taiwan.
CONCLUSIONS
1 . Biostratigraphy and stratigraphic correlation
in Taiwan was studied with framework
mainly based on F oramin ifera in the last
decades. Recently, the same work on Gal-
careous nannop lankton has been carried out
and successfully applied to
oil
exploration.
2. Based on the studies, a total of 24 calcareous
nannoplankton datums and 20 nanno-
biostratigraphic zone have been recognized
and summarized. Correlations can be made
among the sections and basins, as well as
with the standard
in
north Taiwan.
3. The boundaries of the Oligocene and Mi-
ocene, Miocene and Pliocene, and Pliocene
and Pleistocene can be suggested based on
the nannoplankton study.
4.
There are three major unconformities that
have been recognized from the Coastal
Range, eastern Taiwan. One is on the base
of the Lower Miocene sediments, or the
so-called Pachangchi Sandstone, in the
Peikang area, which agrees with the h l i
orogeny. The second is on the top of the
Middle Miocene sediments, or on the top
part of the socalled Nanchung Formation,
which is a local unconformity limited to the
Peikang area. The third one is on t he top of
the Early Pleistocene, or within the socalled
Toukoshan Formation, which might be cor-
related w ith a part of the Penglai Orogeny in
Taiwan. Another unconform ity is recognized
from the to p of the Late Miocene Tuluanshan
Formation.
5 .
Th e biostratigraphic data of the Coast
Range, eastern Taiwan, not only can be
made use of for stratigraphic correlations,
but can also provide evidences of the strati-
graphic record of the plate interactions of
the Philippines Sea plate and the South
China plate. However, the tectonic move-
me nt of th e C oast Range and its relations
with western Taiwan and some other Pacific
regions call for still more detailed study.
ACKNOWLEDGEMENTS
The write r would like to express his gratitude
to Mr. T.M. Wu, Vice President of the Chinese
Petroleum Corporation and Dr.
S.L.
Chang,
Director of the Exploration and development
Research Center
C
.P.C. for their continuous
encouragement and discussions through the
study. I also thank Professor C.S. Ho, advisor
to MRSO for his critical reading of the manu-
script and helpful suggestions. Thanks are
extended to all my colleagues of the Micro-
paleontology Laboratory, exploration and
Development Research Cente r, Chinese
Petroleum Corporation, for their field work
and laboratory assistance.
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