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Integrated geophysical investigation of the Karoo Basin, South AfricaScheiber-Enslin, Stephanie E 10 May 2016 (has links)
A thesis submitted to the Faculty of Science, University of the Witwatersrand,
Johannesburg, in fulfilment of the requirements for the degree of Doctor of
Philosophy
Johannesburg, August 2015
School of Geosciences, University of the Witwatersrand / The possibility of extensive shale gas resources in the main Karoo Basin has
resulted in a renewed focus on the basin, and particularly the Whitehill Formation.
The main Karoo Basin has been the subject of geological studies since before the
1920s, but geophysical data provides an opportunity to shed new light on the
basin architecture and formation. In this thesis, I use regional gravity, magnetic
and borehole data over the basin, as well as vintage seismic data in the southern
part of the basin. Modern computational capacity allows for more information to
be extracted from these seismic data, and for these data to be better integrated
with potential field data. The integration of datasets in a three-dimensional model
(3D) has allowed for a better understanding of the shape of the basin and its
internal structure, in turn shedding light on basin formation.
A new depth map of the basin constructed using this extensive database
confirms that the basin deepens from on- to off-craton. The basin is deepest along
the northern boundary of the Cape Fold Belt (CFB), with a depth of ~4000 m in
the southwestern Karoo and ~5000 m in the southeastern part of the basin.
Sediment thickness ranges from ~5500 to 6000 m. The Whitehill Formation along
this boundary reaches a depth of ~ 3000 m in the southwest and ~4000 m in the
southeast. Despite limited boreholes in this region, the basin appears to broadly
deepen to the southeast. These seismic and borehole data also allow for mapping
of the Cape Supergroup pinch-out below the Karoo basin (32.6°S for the
Bokkeveld and 32.4°S for the Table Mountain Group), with the basin reaching a
thickness of around 4 km just north of the CFB. The gravity effect of these
sediments in the south is not sufficient to account for the low of the Cape Isostatic
Anomaly near Willowmore and Steytlerville. This ~45 mGal Bouguer gravity low
dominates the central region of the southern Karoo at the northern border of the
CFB. The seismic data for the first time show uplift of lower-density shales of the
Ecca Group (1800 – 2650 kg/m3) in this region, and structural and seismic data
suggest that these lower density sediments continue to depth of 11 to 12 km along
normal and thrust faults in this region. Two-dimensional density models show that
these shallow crustal features, as well as deeper lower crust compared to
surrounding regions, account for the anomaly.
These seismic and borehole data also allow for constraints to be placed on
the distribution and geometry of the dolerite intrusions that intruded the basin after
its formation, and in some cases impacted on the shale layer, to be constrained. The
highest concentrations of dolerites are found in the northwest and east of the basin,
pointing towards two magma sources. The region of lowest concentration is in the
south-central part of the basin. Here the intrusions are confined to the Beaufort
Group, ~1000 m shallower than the shale reservoir, suggesting it should be the
focus of exploration efforts. These dolerite sills are shown to be between 5 and 30
km wide and are saucer-shaped with ~ 800 m vertical extent, and dips of between
2° and 8° on the edges. The sheets in the south of the basin extend for over 150
km, dipping at between 3° and 13°, and are imaged down to ~ 5 km. This change
in dip of the sheets is linked to deformation within the Cape Fold Belt, with
greater dips closer to the belt, although these sheets do not appear to intrude strata
dipping at more than 15 to 20°.
In order to understand the shape of the Karoo basin and construct a 3D model
of the basin, an understanding is needed of the underlying basement rocks. The
Beattie Magnetic Anomaly (BMA) that stretches across the entire southern part of
the basin forms part of the basement Namaqua-Natal Belt. Filtered magnetic data
confirm that the Namaqua and Natal Belts are two separate regions with different
magnetic characteristics, which is taken into account during modelling. The BMA
is shown to be part of a group of linear magnetic anomalies making up the Natal
Belt. The anomaly itself will therefore not have an individual effect on basin
formation, and the effect of the Natal Belt as a whole will have to be investigated.
An in-depth study of outcrops associated with one of these linear magnetic
anomalies on the east coast of South Africa suggest the BMA can be attributed to
regions of highly magnetic (10 to 100 x 10-3 SI) supracrustal rocks in Proterozoic
shear zones. Along two-dimensional magnetic models in the southwestern Karoo
constrained by seismic data, these magnetic zones are modelled as dipping slabs
with horizontal extents of ~20-60 km and vertical extents of ~10-15 km. Body
densities range from 2800- 2940 kg/m3 and magnetic susceptibilities from 10 to
100 x 10-3 SI.
These, as well as other geophysical and geological constraints, are used to
construct a 3D model of the basin down to 300 km. Relatively well-constrained
crustal structure allows for inversion modelling of lithospheric mantle densities
using GOCE satellite gravity data, with results in-line with xenolith data. These
results confirm the existence of lower density mantle below the craton (~3270
kg/m3) that could contribute to the buoyancy of the craton, and an almost 50
kg/m3 density increase in the lithospheric mantle below the surrounding
Proterozoic belts. It is this change in lithospheric density along with changes in
Moho depths that isostatically compensate a large portion of South Africa’s high
topography (<1200 m). The topography higher than 1200 m along the edge of the
plateau, along the Great Escarpment, are shown to be accommodated by an
asthenospheric buoyancy anomaly with a density contrast of around 40 kg/m3,
while still mimicking the Bouguer gravity field. These findings are in line with
recent tomographic studies below Africa suggesting an “African Superplume” or
“Large Low Velocity Seismic Province” in the deep mantle.
The basin sediment thickness maps were further used to investigate the
formation of the main Karoo Basin. This was accomplished by studying the past
flexure of the Whitehill Formation using north-south two-dimensional (2D)
profiles. Deepening of the formation from ~3000 m in the southwest to ~4000 m
in the southeast is explained using the concept of isostasy, i.e., an infinite elastic
beam that is subjected to an increasing load size across the Cape Fold Belt. Load
height values increase from 4 km in the southwest to 8 km in the southeast. This
larger load is attributed here to “locking” along a subduction zone further to the
south. The effective elastic thickness (Te) of the beam also increases from around
50 km over the Namaqua and Natal Belts in the southwest to 80 km over the
Kaapvaal Craton and Natal Belt in the southeast. The changes in Te values do not
correlate with changes in terrane, i.e., a north to south change, as previously
though. The large extent and shape of the Karoo basin can therefore, in general,
be explained as a flexural basin, with the strength of the basement increasing
towards the southeast. Therefore, while factors such as mantle flow could have
contributed towards basin formation, reducing the load size needed, it is no longer
necessary in order to account for the large extent of the basin. This flexure model
breaks down further to the southeast, most likely due to a very high Te value. This
could be the reason for later plate break in this region during Gondwana breakup.
It is inferred that this increase in Te is linked to the buoyancy anomaly in the
asthenospheric mantle.
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Tectonic influence on the evolution of the Early Proterozoic Transvaal sea, southern AfricaClendinin, C W 14 January 2015 (has links)
The epeiric Transvaal Sea covered the Kaapvaal Craton of
southern Africa during the Early Proterozoic and its remnant
strata represent one of the oldest known carbonate depositories.
A genetic stratigraphic approach has been used in this research
on the evolution and syndepositional tectonics of the Transvaal
Sea; research also emphasized the development of basement
precursors, which influenced the Transvaal Sea. Eight subfacies
were initially recognized and their interrelationships through
Transvaal Sea time and space were used to identify ten
depositional systems. Paleogeographic reconstructions indicate
that the depositional systems developed on morphological
variations of a distally-steepened carbonate rarp and that the
depositional character of each was simply a function of water
Backstripping of the depositional systems indicates that the
Transvaal Sea was compartmentalized; three compartments are
preserved on the Kaapvaal Craton. Backstripping also indicates
that the depositional center of the Transvaal Sea lay over the
western margin of an underlying rift. Rifting had developed a
major, north-south-trending structure, and its geographical
interrelationships with the east-west-trending Selati Trough
created the compartment architecture of the basement.
Interpretation of syndepositional tectonics suggests that
six stages of subsidence influenced the Transvaal Sea. Early
subsidence consisted of mechanical (rift) subsidence followed by
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The nature of the western margin of the Witwatersrand BasinVan der Merwe, Roelof 07 October 2014 (has links)
D.Phil. (Geology) / The tectonic evolution of the "western margin" of the Witwatersrand Basin is examined and indications are that it has undergone a long and complex history. In order to examine the nature of Witwatersrand-age structures, structures in both pre- and post-Witwatersrand sequences are also examined. Rocks of the ±3074 Ma Dominion Group were subjected to a tectono-metamorphic event prior to the deposition of Witwatersrand strata on an angular unconformity. An oligomictic conglomerate is sporadically developed at the base of the Witwatersrand Supergroup. PreVentersdorp structures in Witwatersrand strata are developed in two distinct trends, north-south and northeast-southwest. The relationship between the two directions of folds and thrust faults are best explained within a regional, sinistral transpressive shear couple; the north-south faults are sinistral strike-slip faults and the northeast-southwest trending folds and thrust faults are secondary structures associated with the strikeslip faults. The implications of this model are that Witwatersrand sedimentation was probably controlled by lateral movements on north-south trending faults and not by thrust faults in a foreland system as suggested by the most recent models of Witwatersrand basin development. Post-Witwatersrand deformation is complex. Southeastward verging, pre-Ventersdorp, thrust faults were reactivated as normal faults during Platberg times and the resultant half-grabens were infilled by conglomerates of the Kameeldoorns Formation. Later deformational events include eastward verging post-Ventersdorp thrust faults and post-Transvaal normal and strike-slip faults. It can be demonstrated that the majority of this later fault movements took place along pre-existing fault planes and therefore tectonic inversion is a fundamental process in the evolution of the Witwatersrand Basin. Clearly therefore, the present distribution of Witwatersrand strata does not reflect the original basin geometry, it is the result of several periods of basin inversion and no basin margins can be defined.
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Basinfill of The Permian Tanqua depocentre, SW Karoo basin, South AfricaAlao, Abosede Olubukunola 03 1900 (has links)
Thesis (MSc)--Stellenbosch University, 2012. / ENGLISH ABSTRACT: Basin subsidence analysis, employing the backstripping method, indicates that
fundamentally two different basin-generating mechanisms controlled Tanqua depocentre
development in SW Karoo Basin. The subsidence curves display initial dominantly
decelerating subsidence, suggesting an extensional and thermal control possibly in a strikeslip
setting during the depocentre formation; on the other hand, subsequent accelerating
subsidence with time suggests that the dominant control on the depocentre formation in SW
Karoo was flexure of the lithosphere. Based on these observations on the subsidence
curves, it is possible to infer that the first stage of positive inflexion (~ 290 Ma) is therefore
recognised as the first stage of Tanqua depocentre formation.
Petrographic study show that most of the studied sandstones of the Tanqua depocentre at
depth of ~ 7.5 Km were subjected to high pressure due to the overlying sediments. They are
tightly-packed as a result of grains adjustment made under such pressure which led also to
the development of sutured contacts. It is clear the high compaction i.e. grain deformation
and pressure solution occurred on the sediments; leading to total intergranular porosity
reduction of the quartz-rich sediments and dissolution of the mineral grains at intergranular
contacts under non-hydrostatic stress and subsequent re-precipitation in pore spaces.
Furthermore, siliciclastic cover in the Tanqua depocentre expanded from minimal values in
the early Triassic (Early to Late Anisian) and to a maximum in the middle Permian (Wordian
-Roadian); thereby accompanying a global falling trend in eustatic sea-level and favoured by
a compressional phase involving a regional shortening due to orogenic thrusting and positive
inflexions (denoting foreland basin formation). The estimate of sediment volume obtained in
this study for the Permian Period to a maximum in the middle Permian is therefore
consistent with published eustatic sea-level and stress regime data. In addition, this new
data are consistent with a diachronous cessation of marine incursion and closure of Tanqua depocentre, related to a compressional stress regime in Gondwana interior during the late
Palaeozoic. / AFRIKAANSE OPSOMMING: Die ontleding van komversakking met behulp van die terugstropingsmetode bring aan die lig
dat die ontwikkeling van die Tankwa-afsettingsentrum in die Suidwes-Karoo-kom hoofsaaklik
deur twee verskillende komvormende meganismes bepaal is. Die versakkingskurwes toon
aanvanklike, hoofsaaklik verlangsaamde versakking, wat daarop dui dat ekstensie- en
termiese beheer gedurende die vorming van die afsettingsentrum plaasgevind het,
waarskynlik in strekkingwaartse opset. Aan die ander kant toon daaropvolgende
versnellende versakking wat mettertyd plaasgevind het dat die vorming van die
afsettingsentrum in die Suidwes-Karoo eerder oorwegend deur kromming van die litosfeer
beheer is. Op grond van hierdie waarnemings met betrekking tot die versakkingskurwes, kan
mens aflei dat die eerste stadium van positiewe infleksie (~ 290 Ma) dus as die eerste
stadium van die vorming van die Tankwa-afsettingsentrum beskou kan word.
Petrografiese studie toon dat die meeste van die sandsteen wat van die Tankwaafsettingsentrum
bestudeer is, op diepte van ~ 7,5 Km aan hoë druk onderwerp was
weens die oorliggende sedimente. Die sandsteen is dig opmekaar as gevolg van die
korrelaanpassing wat onder sulke hoë druk plaasvind, wat op sy beurt ook tot die
ontwikkeling van kartelnaatkontakte aanleiding gegee het. Dit is duidelik dat die sediment
aan hoë verdigting, dit wil sê korrelvervorming en drukoplossing, onderwerp was, wat gelei
het tot algehele afname in interkorrelporeusheid by die kwartsryke sedimente; die
ontbinding van die mineraalkorrels in interkorrelkontaksones onder niehidrostatiese
spanning, en daaropvolgende herpresipitasie in poreuse ruimtes.
Voorts het silisiklastiese dekking in die Tankwa-afsettingsentrum toegeneem van minimale
waardes in die vroeë Triassiese tydperk (vroeë tot laat Anisiaanse tydperk) tot hoogtepunt
in die mid-Permiaanse tydperk (Wordiaans–Roadiaans). Dié ontwikkeling het
gepaardgegaan met algemene dalingstendens in die eustatiese seevlak, en is verder
aangehelp deur saamdrukkingsfase wat gekenmerk is deur regionale verkorting weens orogeniese druk en positiewe infleksies (wat met voorlandkomvorming saamhang). Die
geraamde sedimentvolume wat in hierdie studie vir die Permiaanse tydperk bepaal is, met
die hoogtepunt in die middel van dié tydperk, is dus in pas met gepubliseerde data oor die
eustatiese seevlak en spanningstoestand. Daarbenewens strook hierdie nuwe data met
diachroniese staking van mariene instroming en die afsluiting van die Tankwaafsettingsentrum
wat met spanningstoestand in die Gondwana-binneland gedurende die
laat Paleosoïkum verband hou.
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