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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

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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.


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


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


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


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


(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


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


Deflandre

(1 5) The LAD of


(Roth and Hay)

(16) The appearance of Catinaster coalitus

Martini and Bramlette or Discoaster

bollii Martini and B ramlette

(17) The FAD of


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


(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:


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:


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


8/39

352

(7)

Sphenolithus ciperoensis Zone

Definition

:

The LAD of

Sphenolithus distentus

Bram-

let te and Wilcoxon

to

the LAD of

S. ciperoensis


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


the assemblage is the same as plus S.

ciperoensis

Bramlette and Wilcoxon and

Triquetrorhabdulus

carinatus

Martini.

Remarks:

This zone is approximately equivalent to

the


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


(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


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:


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:


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


Sphenolithus

sp.,

Discoaster druggii

Bramlette

and Wilcoxon,


(Hay

and Mohler) or

H. carteri

(Wallich) H.

amplia-

perta


H. intermedia

(Martini),

Discolithina sp., Braarudosphaera

bigelowi

(Gran and Braarud).

Remarks

:


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


9/39

353

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


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


D. varia-

bilis

Martini and Bramlette,

D. formosus

Martini and W orsley, and

Discoaster

‘sp.

Remarks:


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:


Bramlette and

Wilcoxon, H.

kamptneri

(Hay and Mohler).

H. carteri

(Wallich), H

euphratis

Haq,

H.

obliqua


Coccolithus

pelagicus

(Wallich),

C.

miopelagicus

Bukry,


(Roth and Hay),

Sphnolithus heteromophus

Deflandre, S.

conicus

Bukry, S.

pacificus

Martini, S. mori-

forms

(Bronnimann and stradner),

Discoaster

deflandrei


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)


Zone

Definition:


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-


Sphenolithus

belemnos

Bramlette and Wilcoxon t o the LAD

of


Bramlette and

Wilcoxon. and

Discoaster

sp.

drei

-Bramlette and Wilcoxon,

D. variabilis


D. exilis

Martini and

Bramlette,

D. formosus

Martini and Worsley,


10/39

Remarks:


the upper part of the Talu Shale to the basal

part of the Kuanyinshan Sandstone in Northern

Taiwan.

13) Cyclicargolithus loridanus Zone

Definition


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:


(Roth and Hay),

Sphenolithus pacijicus

Martini,

S. rnorifonnis

fonnis (Bronnimann and Stradner), Helicos-

phaera kamptneri (Hay and Mohler), Q c l o -

coccolithina macintyrei


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


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),



Coronocyclus nitescens

(Kamptner), Discoaster of D. kuglen Martini

and Bramlette, D. bollii Martini and Bramlette,

D. varialilis Martini and Bramlette, D. varialilis


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


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.


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:


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;


11/39

355

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. ,


(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


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:


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-


12/39

356

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:


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


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:


Reticulofenestra

pseudoumbilica

(Gartner) to the FAD of


13/39

357


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


[(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:


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


14/39

358

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


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)


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).


15/39

359

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


16/39

360

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


17/39

36 1

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


18/39

362

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.

REFERENCES

AKER, W.H.,

1965,

Pliocene-Pleistocene b oun-

dary, Northern Gulf of Mexico: Science,

vol. 149,110.3685, p. 741-742.

BERGGREN, W.A., and

VAN

C O W E R I N G ,

J.A., 1974, The Late Neogene: biostrati-

graphy geochronology , nd paleoclimatology

of marine and continental stratigraphies

for the past

1 5

million years: Palaeogeogr.,


19/39

363

Palaeoclimat

.

Palaeoecol.,

vol . 1 6 , p .

1

2 16 . , 1979(a), Calcareous nannoplank-

ton biostratigraphy

of the Nantou Area,

G’D’’ HSIEN’ S’H* ’ Central Taiwan: Petrol. Geol. Taiwan, no.

KIND, E.G., SCH REIB ER, A., arid TANG,

p.

136-165.

C.H., 19 70 , Aeromagnetic survey of offshor e

Taiwan:

CCOP Technical Bulletin,

ECAFE, , 1979(b), Calcareous nannoplank-

V O ~ .

, p. 1-34. ton biostratigraphy of the Hunghuatzu

section, Kaohsiung Area: Jour. Explo.

19 67 , Middle Tertiary calcareous nanno -

with English abstract).

plankton of the Cipero section, Trinidad,

W 1 :

Tulane Stud. Geol.,

vol.

5 ,

p,,93-132. , 1979(c), A biostratigraphic study

of the Late Neogene sediments in the Kaoh-

BUKRYs

D j 1971 Ceno zoic siung area based

on

calcareous nannofossils:

nannofossils from the Pacific Ocean:

San

proc. Geol.

sot.

China, no. 2 2 ,

p .

121-144.

Diego

Soc.

Nat. Hist. Trans.,vol. 16, no. 1 4 ,

D . 303-328.

,

1979(d), The nannofossils and

B0SUM7 w’’

BRAMLETTE

M.N*,

and

w’LcoxoN, J‘A.,

Produc. Re.. no . 2, p. 41-54 (in Chinese

, 1973, Low-latitude coccolith

biostratigraphic zona tion: In Ed gar, N.T.,

Saunders, J.B., et al., 1 9 7 3 , Initial Reports

of the Deep Sea Drilling Project, vol. 15 ,U S .

Government Printing Office. Washington,

D.C..

D.

685-703.

their environment significance from the

alleged “Piling Shale” and “Pachangchi

Sandstone” in the Taihsi Structure, Yunlin

Area: Ti-Chih,vol. 2 , p. 25-29. (in Chinese

with English abstrac t).

,

1980(a), Calcareous nannoplank-

CHANG, L.S.. 19 67 , TErtiary biostratigraphy

of Taiwan and its correlation: In KOTORA

HATAI (ed.), Tertiary correlation and cli-

matic changes in the Pacific,

p. 57-65.

,

19 75 , Biostratigraphy of Taiwan:

Geology and Palaeontology of Southeast

Asia,vol. 1 5, p. 337-361.

CHEN. P.H.,

HUANG,

C.Y. HUANG, T.C.,

and TSAI, LP . , 197 7, A study of the Late

Neogene marine sed iments of the Chishan

Area, Taiwan: Paleomagnetic stratigraphy,

Biostratigraphy, and Paleoclimate : Memoir

of the Geology Society

of

China,

no.

2 ,

p .

169-190.

CHI, W.R., 1978(a), The Late Neogene nanno-

, 1980(b), Biostratigraphy of Pei-

kang area: in Chang,

L.S., et al.,

Oil

and Gas

Exploration

in Peikang Area (Part l ) , Geo-

logy and Geophysics, 36 page (in Chinese).

CHI,

W.R.,

1980(c), The biohorzons of the

Operculina

l imestone,

Orbitoid

l imestone,

and

Molluscan

l imestone in the Subsurface

sediments from the Peikang-Yunlin Area:

Ti-Chih, vol.

3 ,

(in Chinese with English

abstract).

, 1980(a), The calcareous nanno-

fossils of the Lichi melange and their signi-

ficance in the interpretation of plate-tectonic

of the Taiwan Region: Ti-Chih, vol . 4 , ( in

Press)

,

NAMSON, J., and SUPPE, J.,

198 (b), Stratigraphic Record of plate inter-

actions in Coastal Range. Eastern Taiwan.

biostratigraphy in the Tainan foothills

re@on’ Southern Taiwan: Geol*

Taiwan, no. 1 5 , p. 89-125.

,

1978(b), Calcareous nonnofossils

and their significance of the Lushan Forma-

tion, Liukuei, Kaohsiung Area:

Mining

Technology vol. 1 6, nos. 10-12, p. 466-

469 (in Chinese).

Memoir

of

the G eologic3’Society of China,

no.

4 , (in Press).

,

and ME I, W.W., 19 80, The nanno -

fossil study of the Shangtao and Pilingchi


20/39

364

sections in Miaoli area. Jour. Explo. Produc.

Res. no . 3 (in press).

CHOU, J.T., 19 65 , Isopachous variations of the

Miocene formations in the Miaoli Region,

Taiwan.

Proc. Geol. SOC.China,

no. 8 , p .

ERICSO N, D.B., EWING,

M.,

and W OLLIN, G.,

1963, Pliocene-Pleistocene boundary in

deep-sea sediments: Science, 139 (3556):

GARTNER,

S. ,

1973, Absolute chronology of

the Late Neogene calcareous nannofossils

succession in the Equatorial Pacific: Geol.

SOC.Amer. Bull., vol. 84, p. 2021-2034.

, 19 77 , Calcareous nannofossil bio-

stratigraphy and Revised zonation of the

Pleistocene :

Marine micropaleontology,

vol.

HAQ, B.U., and BERGG REN, W.A., 19 78 , Late

Neogene calcareous plankton biostratigraphic

of the

Rio

calcareous nannoplankton biostratigraphy and stratigraphic correlation of the mesozoic and cenozoic...

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