Mesozoic and Cenozoic tectonic evolution of Scania, southern Sweden

TecionophMcs, Elsevier

137 (1987) 7-19

Science Publishers

B.V.. Amsterdam

Mesozoic

- Printed

in The Netherlands

and Cenozoic tectonic evolution southern Sweden ERIK NORLING

’ and JAN BERGSTROM

of Scania,

’

’ Geological Survey of Sweden, P.O. Box 670, S-75128 Uppsala (Sweden) ’ Geological Survey of Sweden, Kiliansgatan 10. S-22350 Lund (Sweden) (Received

December

18. 1985; accepted

April 18.1986)

Abstract Norling,

E. and Bergstrom,

Ziegler (Editor), Triassic Scania.

J., 1987. Mesozoic

Compressional

to Early Cretaceous

Late Cretaceous

major basement

blocks.

Intra-Plate transtensional.

dextral,

tectonic

in the Alpine

sinistral

transpressional

The resulting

and Cenozoic Deformations

tectonics

deformations

structural

zone and

involving

Early

the

Palaeozoic,

sediments.

Main

are

from

Permo-Carboniferous,

known

the

Late Triassic-Jurassic, gene. Lack of Devonian evaluate the possibility

deformation

the subsidence

the inversion

and Nielsen, wrench-faulting

Precambrian Mesozoic

Palaeogene

southern

Sweden.

In: P.A.

Tectonoph_vsics, 137: 7-19. of fault-bounded

of these basins

basins

in

and the uplift

of

prep.). This was accompanied by considerable faulting. Upper Silurian deeper water elastics may have been thousands of metres thick (cf. Buchardt

In southern Sweden the margin of the East European Platform corresponds to a complex basement

induced

induced

of Scania.

Foreland.

relief is of the order of 2000 m.

Introduction

block-faulted

evolution

blocks

and

ernmost sandstone previously

truncation

of the Lower

series. These are now preserved

the Central

the

and Cretaceous-Palaeorocks makes it difficult to of Devonian deformation.

Permo-Carboniferous in the uplift of basement

and the profound

Palaeozoic

phases

1985). resulted

Colonus

Scania found

and

Shale Trough,

considered

in southwest-

in the Kattegat

in a boring

only in

(Fig.

in the Han6

to be of Cambrian

2; a

Bay and age is

The most significant lineaments are trending NW-SE in both basement and sedimentary cover.

Mesozoic, presumably Upper Triassic). These wrench deformations which were associated with

Main tectonic elements of Scania and adjacent areas are given in Fig. 1. During the Early Palaeozoic Scania formed part

the

of the vast shelf area facing the rising orogen of the Scandinavian and North Sea-Polish Caledonides.

Early Palaeozoic

marine

sediments,

ranging

in age from Cambrian to Early Silurian, form in Scania a comparatively thin and originally even cover. During the Late Silurian, Scania formed part of the foredeep of the North Sea-Polish Caledonides and became tilted to the south (Nielsen and Vejbaek, in prep.; Bergstrom et al., in 0040-1951/87/$03.50

se. 1987 Elsevier

Science Publishers

development

of the

Oslo

Graben

(Ziegler,

1982) induced in Scania an extensive doleritic volcanism. By Early Permian time much of the area was probably covered by sheet flows and volcanic cones. As only feeder dykes of the extrusives are preserved today it must be assumed that a period of extensive erosion preceded the transgressions in the Mesozoic (Bergstrom, et al., 1985). This period probably corresponds to the interval during which the well-known Permian peneplain was formed in Germany and in the North Sea. The Mesozoic and Cenozoic evolution of Scania,

B.V.

h

HAN&

8AY

BAiyti

Fig. 1. Structural framework of Scania with surroundings.

Present distribution

Fig. 2. Distribution of Lower Palaeozoic sediments in Scania and surrounding areas. Dotted line marks the nortbwestun limit of the tight swarm of Permo-Carboniferous dolerite dykes, apparently cut off (offset?) by the western fault of the Rmme Graben. New evidence suaests that the Mesozoic in the Han6 Bay rests directly on the basement. A level previously thought to represent Cambrian sediments may be clay-weathered basement rocks. (From Bergstram et al., 1982; Larsson, 1984: Bergs&m et al., in prep.)

9

as presented

below,

tion

surveys,

seismic

ploration crops.

wells These

data

Cretaceous

trolled

illustrate

that

tectonics

during

Late Cretaceous structural

was times

inversion

ment.

Lower

Scania

in two major areas, namely

of out-

Shale

Scania

was af-

western

the Triassic by

regional

by a phase

of

the Colonus

The extent

tionally According

The axis of this inversion

locally

and

Danish

part

(e.g., in completely

rocks northeast

of

is preserved

(Fig.

(1980), the Triassic

3). may

of 5000 m in the axial

Embayment.

of this Triassic

However.

basin

is shallow.

the A

maximum thickness of around 700 m is recorded in deep wells in southwest Scania. During the

Triassic Danish

sediments

are extensively

Embayment

and

along

developed

in

subsidence

the Fennos-

candian Border Zone. Beneath Denmark conformably on the Zechstein evaporites

basin,

they rest (Pegrum,

of the marginal

Late Palaeozoic

came reactivated.

(Fig. 1: also Bolau, Norling,

I 1

Fig. 3. Present

of the Triassic

base-

be-

of such are the NW-

trending Kullen-Ringsjon-Andrarum zone. as well as the Svedala and

zoic rocks and the Precambrian

crystalline

parts

fault zones apparently

Examples

1984, p. SO). In the area of the Fennoscandian Border Zone, however, they onlap Lower Palaeo-

Bergstriim

little

to Berthelsen

of the

7) or are

et al. deposits

may have been deposi-

exceed a thickness

Scanian

Triassic

Fig.

basement

of Triassic

Shale Trough

limited,

area of south-

in Bergstrom

Graben,

Alnarp

and finally

across Scania.

(Bergstrom

in

in the Colonus

these two areas Triassic

the

missing.

are preserved

in the Malmii

on the crystalline

in

Cretaceous

series

rest directly

part

the

Scania

Embayment

the Late

and

1982). Between

to

of fault-con-

succeeded

Palaeozoic

Trough

the Danish during

and the Early Tertiary. zone can be traced

ex-

study

time. This period

towards

reflec-

of numerous

the intensive

subsidence

downwarping

on extensive

the results

and

fected by tensional Early

is based

1973; Bergstrom

dislocation Malmo faults et al., 1982:

1985).

I Q ,&

distribution

et al., in prep.).

of Triassic

’

sedimenta

(except

2’km

for the Rhaetian)

m

Present

in Scania

dstrlbution

and surrounding

areas (Rergstrism

et al., 19X7:

In

Scania

menced lation

the

of Triassic

Palaeozoic Middle

Mesozoic

in its southwestern elastics

sedimentation

directly

series. Strata

Fault

small basin

in the east, the Malmij

Triassic

are known

by the synsedimentary

and the &-esund al.. in prep.).

Lower

to the Lower,

Triassic

from this area. This relatively to be delimited

overlying

belonging

and lower Upper

com-

parts with the accumu-

Fault

Fault

attain

and the Middle

a thickness

to lower Upper

65 to 190 m (excluding

development

to a general

climatic

conditions

(Lidmar-Bergstrom.

1982). The mainly reddish

deposits

brightly

Upper

Svedala

dark greyish and brownish

in the north. basin

et

Lower

Triassic

In Scania

silty

and

sandy,

sediments

Triassic

ern and northwestern

deposits

and Hogan&

of continental

as the Hogan&s

Ziegler.

greyish

Middle

and

and lower

by predominantly

sediments

boundary

to humid

1982;

were succeeded

Triassic-Jurassic

but also

arid

coloured,

tian to Hettangian. clayey,

lowering

from

of the Lower,

of 135 to 220 m

the Kagerod

change

appears

in the west (Bergstrom

In this graben-shaped

strata

only

graben

of a major

of the Rhae-

strata

spanning

comprise

coal and

the

mainly

plant

bearing

to deltaic origin. In westScania

Formation

they are referred (some

to

250 m thick),

Formations). Uppermost Triassic series are around 300 m thick and have a much wider geographic

which is subdivided

distribution,

however, the corresponding succession has not yet been sufficiently described from a lithostrati-

margins

thus illustrating

became

gradually

that the older basin overstepped.

The red and green sandstones

and shales of the

into three well defined

bers (Sivhed, 1984). In central and southern

graphic

point

memScania,

of view.

Lower Triassic were deposited in a continental environment, while the greyish sandstones, shales

The warm and humid climate of the Rhaetian and Jurassic favoured a deep kaolinisation of the

and

crystalline basement (Norling in Daniel, 1978, p. 24; Lidmar-Bergstrom, 1982). The kaolin content

marls

of the Middle

Triassic

are of marine

origin. The Middle Triassic seas transgressed presumably into the area of Scania from the south (Ziegler, 1982). Whether Middle Triassic equivalent strata had an originally wider distribution in Scania

is unknown.

series is developed tinental facies. Apart from ment

of the

The Upper in a sandy,

the indications Triassic

Triassic

Keuper

conglomeratic that

of southwest

con-

the developScania

was

accompanied by synsedimentary faulting, no information is available on its tectonic setting (rifting or wrench

faulting).

has given the mid-Rhaetian clays excellent ceramic properties. These so called Rhaetian fireclays have been mined for centuries in Scania, usually along with two main coal-seams, the upper one of which is taken

to form the lithostratigraphic

between

the Triassic

The

Rhaetian

tectonically a slight

strata

relatively

regional,

boundary

and the Jurassic. were

deposited

under

a

quiet regime which involved

westward

downwarp

towards the Danish Embayment. The Rhaetian to Early Jurassic

of Scania

transgression

of

Latest Triassic and Jurassic

the Tethyan the Central northwestern

Sea which reached northwards into Graben of the North Sea and the part of the Danish Embayment did

In latest Triassic times a new period of tectonic activities started. It was to last until the earliest Cretaceous. At the transition from the Triassic to the Jurassic, during the so called Early Kimmerian (or Cimmerian) tectonic phase (sensu Stille. 1924) rifting and wrench tectonics affected wide areas in northwestern and central Europe (Ziegler, 1982; Pegrum, 1984). This tectonic pulse was of major importance in the structural history of Scania. The very sharp change in the style of sedimentation which occurred during the latest Triassic was not only the effect of a change from local

not affect Scania until Hettangian time. If the Rhaetian tectonic pulse seems to have been weak, several observations of Liassic discordances indicate an increased tectonic activity from the Hettangian onwards (Norling in Bergstrom et al., 1982). In depositional areas where fine-grained Hettangian sediments predominate, the presence of “abrupt” intervals of coarse arkosic sandstones have been interpreted as reflecting increased tectonic activity. Furthermore, records of Hettangian and younger Liassic as well as mid-Jurassic breccias and slump structures in cores from wells

11

drilled

at the margin

of the present

(Fig. 1) seem to indicate partly have

of earthquake also been

character.

taken

structure

Soderas

in the

area

horst. This does not mean, Soderas

Late Cretaceous After

horst

inversion

the deposition

deltaic sediments several marine

however,

is rather

of mainly

transgressions

of

margin

in Toarcian

continental

of the Fennoscandian

(Klingspor,

1976)

indicate

transgressions

invaded

up-

phase resulted

in the early mid-Jurassic

Jurassic,

Scania. Border

new marine

Differential

of non-sedimentation. Jurassic transgression

in

sediSuch revolu-

Zone

raphy upheld by stratigraphic series varying in age. For example, in the Angelholm

Jurassic

strata

(Vilhelmsfalt

sediments in

the

in

(as in Karindal-1 Vomb

Formation,

age)

Trough

and

borehole). the

possibly

Pliensbachian

Late

At Eriksdal Jurassic

This central North Sea High was isolated from the Fennosandian Platform by a narrow zone of sedi-

basement

1981).

to nearshore.

accumulated

coal bearing

in narrow

troughs

sea

transgressed over Middle Jurassic glass sands. In the Assmasa-1 borehole located a few kilometres by sandy layers resting

Polish Trough in the southeast and the North Sea Basin in the northwest (Ziegler, 1982). Limnic-de-

widely Basin

(Figs. 4 and 5) the Oxfordian-Kimmeridgian Fyledal Clay transgressed over truncated Middle

Clay is represented

crossing Scania. This zone formed a at least periodically, between the

and

There followed a Late over a fairly irregular topog-

southwest

ltaic

uplift

occurred

tion was the uplifting of a large rift dome in the central North Sea (Ziegler, 1982, p. 62, encl. 19).

mentation connection,

of dat-

narrow continental-deltaic sedimentary troughs developed isolated from each other by minor areas

became

drastic changes of palaeogeography and mentation patterns in northwestern Europe. change

datings

radiometric

ages of part of the volcanism

Bajocian-Bathonian tectonic

Palynological

the

trending

were

tion and deposition. The mid-Kimmerian

during

NW-SE

of the Fennoscandian

lifted and a long period of marine sedimentation was replaced by a period of continental denuda-

a major

basalts

zone system,

dur-

Scania

the southwest

Shield

of

zones.

were

and Viking

in Scania along

At the end of the Middle

to

times,

transgressions

time,

ings

fault

1973) and K-Ar

Aalenian-Bajocian

of Scania

(Fig. 4).

could indicate hydrothermal processes associated with Early Jurassic faulting. At the end of the Jurassic,

mainly

(Tralau,

parts

Firth

occurred

Jurassic,

that

connected with an increased tectonic activity. Sideritic iron ores along the Fyledal Fault system

Early

activity

Middle tuffites

times.

to Hettangian

These

volcanic

other

As in the Central

the Moray

fault and fracture

the result

invaded

and

day

movements.

in Rhaetian

ing the Early Jurassic.

of a late

since Jurassic

to erosion.

grabens

of the Soderas

of the present

the latter existed continuously The present

subjected

These observations

initiation

At the same time,

horst

movements.

as an indication

Early to mid-Kimmerian horst

Soderas

major crustal

of Eriksdal, (Norling,

The main Upper units, viz. the Fyledal the Vitaback

the base

of the Fyledal on the

Jurassic lithostratigraphic Clay, the Nytorp Sand and

Clays are regionally

correlative

units

and

sands

which are readily recognized in the Vomb Trough, the Landskrona-Helsingborg-Gresund area, and the Angelholm Trough. The axis of the Late

of northern,

west-

Jurassic

clays

sedimentary

Scania trended

in a NW-SE

Angelholm

latest Cretaceous (and presumably Early Tertiary. although this cannot be substantiated within

Bblau,

Trough

1959);

75 m (Vilhelmsfalt

Formation;

Helsingborg-Landskrona-Gresund

flexure zone > 210 m (Fortuna Marl/part/, clay deposits in Gresund, Glass Sand, and the Fuglunda Member-Larsen 1981; Sivhed,

et al., 1968; Norling, 1972; 1984); Fyledalen fault zone 175 m

(Glass Sand and -Sivhed, 1984).

the Fuglunda

Member,

175 m

direction

basin crossing

ern and central Scania and in the Hanij Bay. The following thicknesses of Middle Jurassic strata have been estimated (for location see Fig. 5):

and was apparently

super-

imposed on the Colonus Shale Trough. As discussed below, the latter was subjected to major

Scania) inversion movements which caused more or less complete erosion of the initially thick Jurassic cover (Fig. 5). Where Upper Jurassic strata are still preserved, the following approximate thicknesses have been recorded: Angelholm Trough 163 m (Oxfordian-

Ln.---_I

_.

.

-

,.”

^.

-

.

-

-

_

-_

^

FENN

_.

_

,_

4i.j

_

/_

-,

~~

_

_

-

_-

-

-k

4L

-

:

:

:.,

-

.‘,

1.

.,

-

1’ ::

:‘...*

_

-

-

-

2

-

Nl

_

_

13

Fig. 5. Present

distribution

tar-y faults. The volcanic

Kimmeridgian

of Rhaetian activity

Fyledal

meridgian-Portlandian landian Vitaback

and Jurassic

(“volcanic

Clay:

sedimentaq

rocks in Scania

and surrounding

area” on map) is dated both as Jurassic

80

m,

Kim-

Nytorp Sand: 36 m, PortClays: 47 m); Helsingborg-

changes.

The

have yielded

areas. together

with synsedimen-

and as Cretaceoub.

upper faunas

ceous boundary

part

(Norling,

The Vitaback

of the Vitablck

straddling

Clays

the Jurassic-Creta-

1981).

Clays, comprising

clays, limonitic

Landskrona-hresund flexure zone > 75 m (corresponding lithostratigraphic units have estimated

claystone

thicknesses of > 30 m, 36 m, and > 7 m); Fyledalen fault zone 125 m (corresponding figures are 36

succeeded by clayey, silty and sandy deposits. These facies shifts and differences in the strati-

m, 18 m, and 70 m respectively). (Upper Jurassic thicknesses from Christensen, 1968; Larsen et al.,

graphic representation between tectonic blocks indicate vertical movements and repeated shifts from

1968;

marine to brackish back. These lateral

Daniel,

Norling

and

Skoglund,

1978; and Norling,

1977;

Norling

in

1981, 1982.)

Early Cretaceous As in other parts of Western and Central Europe tectonic activities increased in Scania at the Jurassic-Cretaceous transition (Ziegler, 1982, encl. 38). During this so-called Late Kimmerian tectonic phase, pre-existing faults were reactivated and differential movements of individual fault blocks occurred. The Late Jurassic fairly uniform regional facies pattern was replaced during the Neocomian by a pattern of rapid lateral and vertical facies

and layers of arenaceous

Dramatic

effects

are

and limnic environments and and vertical variations in lith-

ology and representation reflect variations in the Austrian?) tectonic pulse. younger) exposure

marlstone,

of

are here regarded to Late Kimmerian (and Late

Kimmerian

(and

tectonics can be studied in the Eriksdal in the present Vomb Trough where the

Jurassic sequence (including the Vitaback Clays) has been tilted to a vertical position (BBlau, 1973; Norling in Bergstrom et al., 1982: Bergstrom, 1985). A major unconformity has also been observed in cores from Kullemolla-1 borehole southeast of Eriksdal in the Vomb Trough. Here more

Late Cretaceous

or less horizontal Upper Cretaceous strata overlie a steeply dipping sequence underlying the Upper Cretaceous (Gavelin. 1919; Lundegren. 1935; Guy-Ohlson 1982; Chatziemmanouil, 1982). In Scania upper Lower Cretaceous to Cenomanian strata are represented mainly by a laterally fairly continuous sequence of Aptian shales and Albian-Cenomanian glauconitic sands and sandstones, which were deposited during a tectonically fairly calm period (Fig. 6).

Much of Scania appears to have acted as ;i stable tectonic unit during the Turonian-Coniacian interval. In southwest Scania (MalmB area). the Alnarp Graben, and the Vomb Basin, sandstones, marlstones and marly limestones reach a thickness of 140-150 m. In the Han6 Bay, however, the thickness of time equivalent sandy limestones is only about 25 m. and a comparable

Present surface 0

@

End Maastrichtian

_

surface

Maast-richtlan II t Csmpcmlsn Santontan

End Co&Wan

20 m.y. je

surface

- - Coniacian-E.Cretaceous

- -

I 55 m.y.

End Jursssic surface

~ -E==3 Mid Late Trilselc

surfscs Trm38k

N33mien -Scythkn) 20 m.y. Fig. 6. Evolutionary cross-section through southern Scania, separated into tectonic bfock units. B-Lower Triassic (Bun&and&n); M-LK-Middle to lower Upper Triassic (Muschelkalk-Lower Keuper); UK-mid-Upper Triassic (Upper Kcuper, i.e. K&ger&.I M-Maastrichtian. Beds); R--uppermost Triassic (F&aetian); J-Jurassic: S- Santonian: C-Camp&an;

15

situation

could

be present

Corresponding

strata

Kristianstad

area.

strata

which

Turonian

to Coniacian

became units.

areas

total

ero-

it impossible active

to

during

times.

into

Romeleas

deformation,

Scania

a series of new tectonic

Fault

separated

from the Romeleas-Vomb

The northeastern

As a

margin

southwest

block

(Fig. 7).

of this block was formed

locally

along

margin

the

was

uplifted

and

exposed

to erosion

basement

ridge. The

of the most

intense

from block to block. For example,

sediments

differs

the Vomb area mainly

during

down-

the Santonian,

warping

whereas

Campanian

was more pronounced

and

B&tad

tion

is incomplete

basins

(where and

in the Kristianstad

the Maastrichtian absent,

sec-

respectively).

In

southwest Scania downwarping was strong from the Santonian (350 m) through the Campanian the 1983 Geologic

basin

downwarping

and the HanG Bay Basin were downwarped

(400 m) to the Maastrichtian

Scanian

On

part of this block

ultimately

the

southeast

fault-

Vomb Trough.

and now forms the Romeleas

by a fault parallelling the Jurassic Fyledalen Fault but not identical with it. In this way a thin slice of Jurassic

northeastern

of the narrow

the other hand, the southwestern

timing

into the Maastrichtian.

subdivided

Scania

were

of compressional

The

bounded

saw the onset of a new tectonic

which lasted

consequence

deposited

in the

renders

faults

The Santonian regime,

Basin.

to be absent

In intervening

sion of Cretaceous determine

in the B&tad

appear

(up to 700 m). Using

Time Scale (DNAG,

was preserved along part of the Fyledalen structural zone when the eastward adjacent Cretaceous

Am.)

southeast

100 m, 40 m, and 85 m per m.y., respectively, for the three time intervals. The contemporaneous

Scanian

nuded during mineralizations drothermal

block

became

the Late Cretaceous are here thought

activity

raised

and

de-

(Fig. 7). Copper to indicate hy-

along the fault. Further

east the Hanii Bay-Kristianstad Basin along the Christians& the Linderodsasen,

northsubsided and the

for an approximate

mentation

rates,

evaluation

Geol. Sot. of the sedi-

these seem to have been around

uplift of the Romeleas Ridge is evident influx of terrigenous sand into the adjacent Direct evidence obvious in the

of these Fyledalen

by the basins.

tectonic movements is tectonic zone, where

Navlingeasen faults (Fig. 8). A similar situation is evident in the northwest, where the B&tad Basin subsided along a fault separating the Hallandsas Ridge to the south (Fig. 8). The southwest Scanian and Romeleb-Vomb blocks were tilted to the

Jurassic and Cretaceous strata became raised and even overturned by the combined Kimmerian movements and the Late Cretaceous compres-

northeast,

Ohlson,

whilst the Hanii Bay-Kristianstad

Basin

sional

event

Bergstrom termination

Romeleas-Vomb

direct

m of Santonian

to Maastrichtian

sediments

were

movements where

9; Gravesen,

1982). In general

and B&tad Basin blocks were tilted to the southwest. The tilting is most notable in the narrow Block, where at least some 600

(Fig.

of

evidence appear

in

Guy-

to date the

Cretaceous

inversion

alone. The most

is seen in the Kristianstad

movements

to have

Basin. occurred

NE ALNARP GRABEN

HbLLVlKEN

Fig. 7. Simplified

75-81:

it is difficult

Late

from Scanian

evidence no

the

SW

given for Upper

1977; Norling

et al., 1982, pp. 38-41,

and schematic Cretaceous

cross section

is valid throughout.

through Length

the southwestern of section

ROMELEASEN HORST

part of Scania

is about

70 km.

(from

VOMB

Bergstriim

BASIN

et al.. 1987). Vertical

scale

Present

distrububon

Volcanism

Active

fault

Fig. 8. Present distribution of the Cretaceous sediments in Scania and surrounding areas. Note change in faulting compared with the Jurassic, (From Bergstram et al., 1982; Bergstrom et al., in prep.)

TORPAKLINT V

FYLEDAL

AREA T

c

F

V

C

VALLEY

E

directions

as

after the Early Campanian along the NMing&en Horst. As suggested above, tectonic movements persisted, however, much longer in southwest Scania, where the Maastrichtian is particularly thick, and where also the presence of Lower Tertiary strata indicate some sinking in the Early Tertiary.

Fig. 9. Evolution of the Fyledal Fault structure. Left; cross section through the Torpaklint horst (T in inset map) area: right: cross section through the Fy%dal Valley (F) area. A. Deposition of Lower Palaeozoic sediments (LP) throughout Scania. B. Late Palaeozoic wrench faulting, with uplift of the Vomb block (V) and removal of sedimentary cover. C. Leftlateral

transtensional

with lowering

/

IT \

c ”

,

1

F /

slim

\

/

Inversion

during

pressional

wrench

Horst the

Fyledal

the Late Cretaceous, faulting

Valley. but

resulting

and Jurassic

with right-lateral

the approximate

D.

trans-

in the uplift of Torpaklint cross

Jurassic

sections

areas. The cross sections

from inset map.

(TJ ).

Shale Trough).

of thick eastern

E. Present

and Fyledal

to scale.

deduced

during Triassic

block (C -Colonus

(T) and downfaulting

Torpakhnt not

faulting

of eastern

horizontal

series in

through

the

are schematic. scale

can

be

17

Tertiary

still

Marine

sediments

confined

to the

of Tertiary

Paleocene

age are virtually

and

Danish-Polish

Trough

southwest

Fault.

erratics

of similar

Marine

found

also in eastern

appear sider

to be present it as probable

Paleocene

resumption

accompanied by vertical

Scania,

rivers

courses

10; Troeds-

their

sedimentation

subsidence

p.

was

suggested

Tertiary sition).

and the deflection

Lidmar-Bergstrom some

small-scaled

in this area may have occurred

(possibly although

at the Oligocene-Miocene a Late Cretaceous

age for this depression.

by Ziegler

important

features

uplift. This is indicated by the distribution of outliers of Cretaceous sediments and also of Up-

genesis in Scania can be summarized

erratics,

some of which

(1982,

distribution

conditions

of Lower Tertiary

for the Late Tertiary.

(mainly

Thickness

Danian) figures

tran-

events model

38). The more tecto-

as follows:

(1) Triassic to Early Cretaceous tectogenesis along the Tornquist Zone was caused by sinistral

are

I, -I’

Fig. 10. Present

encl.

of the above-described

Present

terrestrial

block in the

origin can not

The character and effects of the tectonic in Scania seem to fairly well fit the tectonic presented

flint

(1982,

Summary of the tectogenesis

The central parts of northern Scania appear to have experienced a comparatively late tectonic

per Cretaceous

from

et al.. 1982, p. 47). The

of Scania

that

(Fig.

for the

be excluded.

faults

valley is filled with up to 125 m of Quaternary sediments, and the absence of upper Tertiary strata a Quaternary

32)

movements

a

(Fig. 8). Southwest of the Romeleas Fault, and parallelling it, lies the Alnarp Valley, which seems to be a graben structure (Figs. 1, 7, 10). This

may indicate

original

of the rivers is unknown.

controlled

along the preexisting

apparent

age of this late uplift

strata Basin

of the Lagan

son, 1928, 1932; Bergstrom

Bay. We con-

in the Han6

of marine

and Helgean

of the

marine

(Lidmar-Bergstrom,

deviation

ages have been

and

position

there is evidence

of the Romeleas

in the Hanii that

by moderate movements

Eocene

in a sedentary

1982, p. 32). Moreover,

strata.

Old

Finds of silicified

refer to the Danian.

rwer

plants

dlstrlbutlon volley

in different

parts of Scania indicate

(left-lateral)

wrench

faulting

(2) Late Cretaceous genesis

along

dextral

(right-lateral)

pression,

the Tornquist

resulting

southwestern

Scania

part

during

Rhaetian

stronger

(5) A peak

and

NW-SE,

became

the Early Jurassic. activities

Jurassic including

orientation

with

faulting

horst and graben

during

peak

Jurassic-Cretaceous

for-

Neocomian.

with

Kimmerian

an

move-

early Middle

Entwicklung

B., Larsson.

K.. Norling,

to excursions

in Scania. Uppsat,

J.. Bless. J.M. and Paproth.

Knabberud

Limestone

Dtsch.

Schoncns

Geol.. 31: 277- 280.

Ser. Ca: Avhandl.

E. and Sivhed. IJn-

Sver. Geol. 54: OS pp.

E.. 1985. The marine

in the Oslo Graben:

for the model

of Silesian

possible

im-

palaeogeography.

2.

Geol. Ges., 136: 181-194.

Bergstrom,

J., Kumpas,

O.V., (in prep.). Tomquist

M.G.,

Evolution

Zone.

Pegrum,

R.M.

and

of the northwestern

Pub].

AbschluDsymp.

Vejbek,

part of the

IGCP-ProJ.

86.

and depositional

his-

4/86.

Berthelsen,

F., 1980. Lithostratigraphy

tory of the Danish

of tectonic

activity

transition

ebbing

Movements

along

at the

away in the pre-existing

Bolau,

Triassic.

Danm.

E., 1959. Der Stidwest-

Schildes F&h., BBlau.

(Schonen

Geol. Unders..

Ser. B.

events

Jurassic,

in central

Scania

Early Cretaceous,

Cretaceous times (Figs. 4, 5, 8). (9) Differential subsidence, including

during and Late

E.,

1973.

Kimmerian tectogenesis. (10) The Late Cretaceous (Santonian-Maastrichtian) involved a major inversion of the movements with the formation of important basins and troughs: the southwest Scanian and Vomb troughs and the Ha& Bay, Kristianstad and B&tad basins and the uplift of major highs such as the Romelehs ridge. The latter was associated

with the

formation of a giant flexure along the boundary between the Danish Embayment and the Fennoscandian Border Zone. (11) The Late Cretaceous

continued

into the Paleocene in the MalmS Trough, but such a continuation is not clearly substantiated elsewhere. (12) A slight rise of northern Scania indicates the possibility of later Tertiary movements of moderate extent. Neotectonics are not known with certainty, but for instance the absence of Upper Tertiary strata in the up to 100 m deep Alnarp trench, parallelling the Romel&en Fault, raises the question of very late movements.

Kimmerischen

B. and Nielsen, composition

Stockh.

Bewegungen

Geol. F&en.

Stockh.

Foren.

Stockh.

A. Th., 1985. Carbon

of Lower

im FGrh..

Evidence F&h.,

carbonate

rocks

of deep burial

diagenesis.

Geol.

106(4) (1984): 383-384.

J., 1982. The Upper Cretaceous

Trough.

geology

Part I: Structure,

II: Foraminiferal tonian

palaeoecology

sequences

Geol., 38(5/6): Christensen, Avhandl. Daniel,

and its applications.

Jurassic 1978.

in Scania.

efter

P.,

till jordartskartan

meddelande

stenkol

Hiiganlis

Ser. Ae, 25: 92 om resultaten

i Sk&e.

Geol.

Foren.

1977.

Nye

iagttagelser

pB

i Sydest-Sk&ne.

kridtlokaliteten

Dansk

Geol.

Foren.,

1976: 75-83.

Guy-Ohlson,

D..

1982.

Jurassic-Cretaceous Sweden. Klingspor,

Biostratigraphy

unconformity

Sver. Geol. Unders., I., 1976. Radiometric

dolerites

and

related

Geol. Fiiren. Stockh. G., Buch,

Oresund.

in Sk&e,

Lower southern

of basalts,

southern

Sweden.

O.B. and Bang,

I., 1968.

98: 195-216.

A., Christensen,

Geol. Rapp. Danm.

1: 90 pp.

K., 1984. The concealed

Geol. Foren.

the

Ser. Ca, 52: 45 pp.

syenite F&h.,

of

at Kullemolla,

age-determinations

Helsinwr-Hiilsingborgiinien.

Geol. Unders.. Larsson,

from Ser. C:

F&h., 41(3): 221-226.

RSdmolla/Tosterup

Larsen,

Contrib.

and microfaunas

NV. Sver. Geol. Unders..

A., 1919. Ett prehminiirt

Arsskr.,

Stockholm

632: 46 pp.

av djupbormingama Stockholm

Part

and San-

Sver. Geol. Under%.

Beskrivning

NO/Helsingborg PP. Gavelin,

of the Coniacian

57-161.

Uppsat.,

E.,

of the Vomb

and sedimentology.

O.B.. 1968. Some deposits

the Upper

and oxygen

Palaeozoic

Chatziemmanouil,

Gravesen,

movements

Die

Bilde Schonens.

from Bomholm.

slight in-

des Baltischen

Geol. F&en.

95: 165-180. Buchardt, isotope

movements, observed in some tectonic (e.g. the Angelholm Trough) during the

und Siidostrand

und Ostbahikum).

81: 167-230.

Tektonischen

(8) Volcanic

Basement

ders.. Arbok,

Potsdam

fault lines.

version blocks

J., Holland,

Bergstrom.

tektonischen

2. Angew.

U., 1982. Guide

plications

in the early block

J., 1985. Zur

(Siidschweden).

4; 59 pp.

ments. (7) Another Late

in

of the Triassic. pulse

Bergstrom, Bergstrom,

trough

mation and a central Scanian volcanism. (6) Formation of transverse troughs ENE-WSW

by

com-

movements.

tectonic

of tectonic

tecto-

was caused

faulting

much

during

of the Middle

trending

Tertiary

of a fault-bounded

(4) A weak successively

Zone

wrench in inversion

(3) Formation

References

and tension.

and initial

Stockh.

F&h.,

Palaeozoic

106: 389-391.

of SW Sk&ne.

19

Lidmar-Bergstrom,

K.. 1982. Pre-Quatemary

cal evolution

in southern

Norling,

geomorphologi-

Fennoscandia.

Sver. Geol.

Un-

stratigraphischen

Ergebnisse

der

A.,

1935.

Tiefbohnmg

Die

bei KullemGlla

Sver. Geol. Unders., Nielsen, zoic

in

Scania,

Denmark

and

southern

and

Foraminifera

of

Sweden. Sver. Geol. Unders.,

Ser.

E.. 1981. Upper

Jurassic

and Lower Cretaceous

geol-

ogy of Sweden. Geol. Fiiren. Stockh. Forh.. 103(2): 253-269. Norling,

E.,

1982.

Langs

Berggrundsgeologiska

stigar

strovtag

mot

det

i Kullabygden.

E..

1984.

palaeogeography

Terra

of Scania.

Cognita.

H.,

Tralau,

H.,

tectonics,

5(2/3):

Siidwestrand

der

Z. Angew.

Troedsson, Stockh.

Geol.

F&en.

and

Stockh.

Fiirh..

and Tertiary 103-104.

evolution

of Scania.

of the Tornquist

biostratigraphy

in Scania,

Zone

in

64: 39-68.

of the Upper

southern

Sweden.

Sver.

Ser. C, 806: 31 pp. Grundfragen

der

vergleichenden

Tektonik.

Berlin. 1973.

En

aktivitet

palynologisk

%ldersbest%mning

i Sk%ne. Fauna

Flora

av

(Stockholm),

4:

121-125.

SkLnes Na-

stratigraphy

and

Jurassic

1924.

Bomtraeger,

G., 1928. Yttrande om strandflaten

med anledning

Ziegler,

av B. Asklunds

p% Sveriges vlstkust.

Geol. Foren.

Forh., 43: 808-810. G., 1932. N%gra tektoniska

lem i Sk%ne. Geol. Wren.

Stockh.

P.A., 1982. Geological

Europe.

E., 1985. Mesozoic

Der

Schwedens.

Sea. Norsk Geol. Tidsskr..

Litho-

Geol. Unders.,

foredrag

106: 393-394. Norling,

U., 1984.

Troedsson, Kimmerian

North

Triassic-Middle

forgangna.

tur, 69: 21-40. Norling,

im Bereich

R.M., 1984. The extension

vulkanisk

Ca, 47: 120 pp. Norling,

R., 1977.

Tafel

the Norwegian

Stille,

stratigraphy

southern

Pegrum, Sivhed,

The Early Palaeo-

of a new hypothesis.

E.. 1972. Jurassic

western

Schonen.

Ser. C, 386: 19 pp.

development

Sweden-outline Norling.

im slidijstlichsten

A.T. and Vejbaek, O.V. (in prep.). basinal

Skoglund,

Geol., 23(9): 449-458.

ders., Ser. C, 785: 202 pp. Lundegren.

E. and

Osteuropaischen

Shell

B.V.-Elsevier,

Intemationale Amsterdam.

Atlas

och stratigrafiska Forh.,

of Western Petroleum

prob-

54: 220-226. and Central Maatschappij

130 pp. and 40 enclosures.