◄ Carnets Geol. 3 (A05) ►
Outline:
[Introduction]
[Historical background]
[Reframing the "Upper Thamama"]
[Interpretations and perspective]
[Conclusions] and ...
[Bibliographic references]
ADMA-OPCO, P.O. Box 303, Abu Dhabi (United Arab Emirates);
present address: Total, DGEP/GSR/VdG, Tour Coupole, 2 Place de Coupole, La
Défense 6 - Cédex 4, 92078 Paris La Défense (France)
ADNOC, P.O. Box 898, Abu Dhabi (United Arab Emirates)
present address: ADMA-OPCO, P.O. Box 303, Abu Dhabi (United Arab Emirates)
Département des Sciences de la Terre, Université Claude Bernard, 15-43 boulevard du
11 Novembre 1918, 69622 Villeurbanne Cedex (France)
ADNOC, P.O. Box 898, Abu Dhabi (United Arab Emirates)
Forschungsinstitut Senckenberg, Senckenberg-Anlage 25, D - 60325 Frankfurt
am Main (Germany)
Manuscript online since July 31, 2003
DOI 10.4267/2042/297
An integrated case study of field "A" in offshore Abu Dhabi found that the stratigraphic framework for the uppermost part of the so-called "Thamama Group" required revision. Detailed sedimentological work permitted a subdivision of the succession into lithostratigraphic units (more accurately "allostratigraphic units") and the fossil content permitted their allocation to standard age-related units ranging from Late Barremian through Middle Aptian times. Additional work focused on the so-called "Shu'aiba Formation" and resulted in a new and comprehensive interpretation on a regional scale which differs from published interpretations based on onshore studies in Abu Dhabi, Qatar, and Oman.
• allostratigraphy;
• lithostratigraphy;
• Cretaceous;
• Hauterivian;
• Barremian;
• Aptian;
• Bedoulian;
• Gargasian;
• Clansayesian;
• Albian;
• Lekhwair;
• Hawar;
• Shu'aiba;
• Bab;
• Sabsab;
• Nahr Umr;
• Abu Dhabi;
• Iraq;
• Qatar;
• Oman
Granier B., Al Suwaidi A.S., Busnardo R., Aziz S.K., Schroeder R. (2003).- New insight on the stratigraphy of the "Upper Thamama" in offshore Abu Dhabi (U.A.E.).- Carnets Geol., Madrid, vol. 3, no. A05 (CG2003_A05), 17 p.
Nouvel aperçu de la stratigraphie du "Thamama supérieur" dans le domaine maritime d'Abou Dabi (Émirats Arabes Unis).- Le découpage stratigraphique de la partie supérieure du "Thamama" dans le domaine maritime d'Abou Dabi nécessitait une révision significative comme cela est démontré avec l'étude intégrée du champ "A". Un travail de détail en sédimentologie a permis de subdiviser cette partie de la série en unités lithostratigraphiques (notons toutefois que le vocable "allostratigraphiques" serait plus précis pour définir ce type de catégories stratigraphiques) alors que la paléontologie permettait leur calage chronostratigraphique dans l'intervalle Barrémien supérieur-Aptien moyen.Un travail complémentaire focalisé sur le "Shu'aiba" a abouti à l'établissement d'une interprétation différente de celles antérieurement publiées qui se basaient sur le domaine continental d'Abou Dabi, ainsi que sur le Qatar ou l'Oman, et qu'il est également possible d'étendre à l'échelle régionale.
• allostratigraphie ;
• lithostratigraphie ;
• Crétacé ;
• Hauterivien ;
• Barrémien ;
• Aptien ;
• Bédoulien ;
• Gargasien ;
• Clansayésien ;
• Albien ;
• Lekhwair ;
• Hawar ;
• Shu'aiba ;
• Bab ;
• Sabsab ;
• Nahr Umr ;
• Abu Dhabi ;
• Iraq ;
• Qatar ;
• Oman
In the
offshore areas of Abu Dhabi (Fig. 1
) the "Thamama Group" includes the uppermost
part of the Sahtan Supersynthem (pro "Group"), the whole of the Kahmah
Supersynthem (pro "Group"), and the lowermost part of the Wasi'a
Supersynthem (pro "Group"). The upper portion incorporates the Kharaib,
Hawar, Shu'aiba, Bab, and Sabsab synthems (pro "formations");
the respective underlying and overlying units are the Lekhwair and Nahr Umr
synthems (pro "formations"). All of these entities were defined from
subsurface data and were correlated more or less successfully throughout the
whole of the southeastern Arabian Gulf oil province (Fig. 2
). Such operational rock
subdivisions were not considered valid lithostratigraphic units until it was recently
demonstrated (Granier, 2000) that they fall into the category of
"unconformity-bounded units" (Salvador, 1987; also known as
"allostratigraphic units"). The surfaces bounding these units are for the most part, but
not always, transgressive surfaces (TS) that are often but not always coincident with
sequence boundaries (SB). Such surfaces are used to obtain precise stratigraphic
correlations between wells in the Abu Dhabi offshore.
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Figure 1:
Location map of United Arab Emirates and its major oil fields. |
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Figure 2:
The relationship of the main reservoir zones to the sequence
stratigraphic subdivisions of the upper part of the so-called
"Thamama". |
To date approximately 4,000 feet of cores have been recovered from 16 of the 43 wells drilled in field "A" in offshore Abu Dhabi. This study documents most of the third order tectono-eustatic cycles that occurred in Barremian through Aptian times. The related stratigraphic sequences and their bounding surfaces provide the elements for the establishment of comprehensive geological models as demonstrated below for the "Shu'aiba".
The
lithostratigraphic framework used in the onshore and offshore areas of Abu Dhabi (Fig. 1
)
was issued by Hassan, Mudd and Twombley (1975) who followed the recommendations
of the "Geological Liaison Committee" formed by several companies
operating in Abu Dhabi, Dubai, Oman, Qatar, and Sharjah, i.e. in the
southeastern Arabian Gulf oil province.
The Lekhwair Formation was first mentioned by Scherer (1969, unpublished report) but it was published only in 1975 by Hassan, Mudd and Twombley. Though the type section was originally chosen in PDO well Lekhwair No. 6 in western Oman, according to Hughes Clarke (1988), well No. 7 should have been selected.
The Kharaib and Hawar formations were first mentioned by Sugden (1953, unpublished report), but were not published until 1975 by Sugden and Standring. The type sections of both formations are in QGPC (ex QPC) well Kharaib No. 1 in central Qatar. In Oman the Hawar Formation has been lumped with the overlying Shu'aiba Formation and in Abu Dhabi with the underlying Kharaib Formation.
The
Shu'aiba Formation was first mentioned by Rabanit (1951, unpublished
report), but was not published until 1958 by Owen and Nasr. The formation was
subsequently redefined by Dunnington, Wetzel and Morton (1959) who reverted to
the original, unpublished description by Rabanit; and by Al Naqib (1967) who
chose to lower the top of the formation considerably. The type section
of the Shu'aiba Formation (Fig. 3 )
is in INOC (ex BPC) well Zubair No. 3 in southern
Iraq. In most Abu Dhabi offshore areas the Shu'aiba Formation has been split into
local sub-units. The upper sub-unit consists of basin deposits with
"Globigerinids" and it has been referred to as the "Bab Member"
by Hassan, Mudd and Twombley (1975). The type section of the Bab Member (Fig.
4 )
is in ADCO (ex ADPC) well Murban No. 2 in onshore Abu Dhabi. In later discussions of this unit
(Al Naqib, 1967), the type Shu'aiba does not include the "Globigerinid" facies.
Consequently the Bab "Member" was upgraded to formational rank (Granier,
2000). Moreover, the base of the type section of the Shu'aiba
Formation still included a time equivalent of the Hawar Formation; therefore the
lower boundary of the Shu'aiba Formation should be raised to exclude the basal 7
foot "pseudo-oolitic limestone" with "Orbitolina discoidea"
(Rabanit, 1951, unpublished report) as well as the thin shaly layer immediately
overlying it (Granier, 2000).
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| Figure 3:
Type section of the Shu'aiba Formation from Rabanit (1951, unpublished
report), modified by Al Naqib (1967) and Granier (2000):
INOC (ex BPC) well Zubair No. 3 in southern Iraq. |
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Figure 4:
Type section of the Bab Formation from Calavan et al. (1992):
ADCO (ex ADPC) well Murban No. 2 in onshore Abu Dhabi. |
The
Sabsab Formation is an informal lithostratigraphic unit (Figs.
5
- 6 ), which was first
published by Sugden and Standring (1975). The type section of the formation is
in QGPC (ex QPC) well Dukhan No. 27 in western Qatar. It was described as an
oolitic, pellety limestone containing abundant abraded orbitolinids. It was
erroneously believed to be channel infills.
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Figure 5:
Example of the Shu'aiba -
Sabsab boundary (here a karst surface and/or an erosional surface) in a platform
setting: South Bu Hasa well No. A in onshore Abu Dhabi from
Russell et al.
(2002), modified. |
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Figure 6:
Example of
both Shu'aiba - Bab and Bab - Sabsab boundaries in a basinal setting: ADMA well No. 4 of
field "B", offshore Abu Dhabi. |
The Nahr Umr Formation was first mentioned by Glynn Jones (1948, unpublished report), and was published by Owen and Nasr (1958). The type section is in the INOC (ex BPC) well Nahr Umr No. 2 in southern Iraq.
Microfossils reported by Banner and Wood (1964), and by Hassan, Mudd and Twombley (1975) refer to obsolete names, such as "Orbitolina cf. discoidea Gras" which presumably include several taxa belonging either to the genus Eopalorbitolina or to the genus Palorbitolina. The same authors also quoted long-ranging species, like Choffatella decipiens (Hauterivian-Aptian), Dictyoconus arabicus (Barremian-Early Aptian; it is now assigned to the genus Montseciella Cherchi et Schroeder 1999[b]), and Salpingoporella (Hensonella) dinarica (Tithonian - Aptian, according to Granier, 2002).
Based on an assemblage of non-coeval species (according to Schroeder et al., 2002) including Eopalorbitolina charollaisi (Hauterivian 7-Barremian 2), Valserina broennimanni (Hauterivian 7-Barremian 1), Dictyorbitolina ichnusae (Hauterivian 7-Barremian 2), and Palorbitolina lenticularis (Barremian 4-Bedoulian 4), Azer and Toland (1993) assign a Barremian age to the base of the Kharaib Formation; this dating and additional fossil identifications, such as "Pseudocyclamina litus" (sic) for instance, are open to question.
In some Abu Dhabi wells, core samples from the uppermost part of the studied interval (i.e. the uppermost Shu'aiba and most of the Bab) include ammonites. Most of the citations listed below seem credible though they are not substantiated by figured specimens nor accompanied by any indication of where the original samples are stored. In the offshore area, specimens identified by Wright (1959, unpublished report; Banner and Wood, 1964; Hassan, Mudd and Twombley, 1975; Azer and Toland, 1993) from "Umm Shaif well No. 2" comprise Cheloniceras (Epicheloniceras) sp., Colombiceras cf. caucasicum, and an ancyloceratinid form. Those identified by Howarth (1992, unpublished report; Azer and Toland, 1993) from "Umm Shaif well No. 3" include cf. Pseudohaploceras sp. and Diadochoceras sp. In addition, Hassan, Mudd and Twombley (1975) reported Pseudosaynella fimbriata, Pseudohaploceras sp., Diadochoceras sp., Gargasiceras sp., and Dufrenoyia sp., possibly from ADCO well Murban No. 2 in the onshore. These findings indicate a Middle Aptian (Gargasian) age.
The sequence stratigraphy of the Upper Thamama by Azer and Toland (1993) was based on three offshore wells ("Umm Shaif No. 88, Zakum No. 182, and Umm Lulu No. 3"). Boichard, Al-Suwaidi and Karakhanian (1994) published another version for the Upper Thamama based on data from field "A". Though there was some agreement on subdivision of the Kharaib Formation, these opinions diverged significantly when dealing with the Shu'aiba Formation. Although both schemes included the Bab Member, Azer and Toland (1993) identified two sequences therein, while Boichard, Al-Suwaidi and Karakhanian (1994) found three.
In his 2000 paper, Granier applied this new stratigraphic classification to the operational units documented in the offshore of Abu Dhabi. The so-called "Thamama Group" covers 9 synthems (i.e. alloformations) which are from top to bottom: Bab, Shu'aiba, Hawar, Kharaib, Lekhwair, Zakum, Belbazem, Bu Haseer, and Habshan. This new classification, which is based on 'unconformity-bounded units', is supported by both biostratigraphic data and sequence stratigraphy. This revised stratigraphic framework suggests that a new interpretation of regional basinal history is necessary.
Although other interpretations have been proposed recently: Sharland et al. (2001), van Buchem et al. (2002), Russell et al. (2002), Davies et al. (2002), none are supported by fresh paleontological findings.
Based on detailed sedimentological and micropaleontological investigations of the wells in "A" field, we propose here a new version of the sequence stratigraphy for the upper part of the Thamama Group.
In the next section, numbers in brackets refer to vertical thicknesses as
recorded in the reference well in field "A"
(Fig. 7 ).
Each depositional sequence is described briefly, using the following abbreviations in
both text and figures: LST = lowstand systems tract, TST = transgressive systems
tract, HST = highstand systems tract.
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Figure 7:
Stratigraphic subdivision of the upper part of the so-called
"Thamama" in the reference well of field "A" (from left to
right: Gamma Ray = red log, Environments = green squares, reversed NPHI = blue
log, reversed RHOB = green log, distribution of the main fossils, third order
sequences, allostratigraphic units).
This figure illustrates how paleontological data may be used to identify (and
quantify) transgressive and regressive trends. Some fossils were chosen as index
fossils: they were given an index value and their occurrence was semi-quantified
(missing, rare, common, abundant). The weighted average was then computed for
their association in each sample. This technique, similar to that developed by
Boisseau, Dupont and Mussard (1990),
is not straightforward since its use
requires hypotheses (which species are the index fossils and what importance
should be ascribed them) and a series of iterative tests in order to obtain the
best (potentially most nearly valid) interpretation. |
Lekhwair Synthem: the uppermost part of the formation consists of mud- and wacke- stones with aragonitic foraminifers (Hensonina and high spired Trocholina) and algae (Cylindroporella, Salpingoporella, Acroporella (?), Terquemella, Carpathoporella, Permocalculus,...), as well as non-aragonitic forms such as Choffatella (foraminifer) and Hensonella (alga). This "aragonitic algal debris facies" is characteristic of an inner platform depositional environment.
The top of the Lekhwair Synthem is marked by a bored hard-ground
(Figs. 8 ,
9 ). It
exhibits strong early diagenesis including an early episode of
lithification that occurred after a burrowing stage and before a boring stage.
This event may have been accompanied by minor subaerial exposure as indicated
by an early leaching of aragonitic bioclasts, with the resulting voids later filled
by sediments.
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Figure 8:
Scan of polished
core (slab). Hard-ground marking the
Lekhwair-Kharaib boundary in well No. 12. |
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Figure 9:
Scan of polished
core (slab). Hard-ground marking the
Lekhwair-Kharaib boundary in well No. 19. |
The Kharaib Synthem is subdivided into 4 cycles, namely, Kharaib-1, 2, 3 and 4.
Kharaib 1: The cycle starts with a very thin transgressive layer (4 ft) of mud-dominated fine-grained packstones, commonly partly dolomitized and locally with sparse quartz silts. The remaining part of this cycle (45 ft) though rather homogenous displays a clear trend of upward shallowing. Its facies consists of wackestones and mud-dominated packstones with foraminifera (high spired Trocholina, Chrysalidina, Hensonina, orbitolinids including Eopalorbitolina transiens (Cherchi et Schroeder 1999[a]) and primitive forms of Palorbitolina lenticularis (Blumenbach) associated with Montseciella arabica (Henson) [in the upper half] and algae (Hensonella, Montiella, Cylindroporella, Carpathoporella, Permocalculus). Such a facies is characteristic of an inner-ramp setting, probably shallower (absence of Choffatella) than the "algal debris facies" found in the Lekhwair Synthem.
The top of the Kharaib 1 cycle is marked by a bored hard-ground, commonly masked by large stylolites associated with the change in texture. At the scale of the field study there is no clear evidence of subaerial exposure.
Kharaib 2: The cycle starts with a transgressive interval consisting of an extremely thin parasequence (2 ft) followed by a thin one (7.5 ft). They are topped by very thin marls sometimes with a coquina at the base. The dominant facies of the cycle are similar to those of the underlying Kharaib 1 HST except for the notable abundance of Choffatella and orbitolinids (Eopalorbitolina transiens and primitive forms of Palorbitolina lenticularis) which records a flooding event, a characteristic of a mid-ramp environment. The remaining part of the cycle (HST) may be subdivided into two slightly regressive parasequences (19.5 ft and 30.5 ft). They are argillaceous mud- and wacke- stones, often slightly dolomitic, with Lenticulina and Choffatella, i.e. an association indicative of a deep- (outer-) ramp setting.
The top of the Kharaib 2 cycle is marked by a burrowed firm-ground. According to micropaleontological investigations carried out over the rather small area studied, we cannot exclude a downward shift of facies from a deep- (outer-) ramp setting below to a mid-ramp setting above.
Kharaib 3: The cycle consists of a thin TST (10 ft) followed by a thick HST
(88.5 ft). The transgressive part of the cycle can be split into 3 very thin
parasequences, each of which has an orbitolinid-rich lag at its base. The
flooding events are marly layers with abundant typical forms of Palorbitolina
lenticularis and common
Choffatella and Lenticulina. If one accepts the
hypothesis of a downward shift, one or two of the three parasequences ascribed
to the TST should be referred to a LST. Though the regressive part of the cycle
is reasonably homogenous it shows a distinct shallowing upward trend. Facies are
rather similar to those found in the Kharaib 1 HST; they consist of wackestones
and mud-dominated packstones with foraminifera (low-spired Trocholina, Chrysalidina,
Hensonina and orbitolinids including typical forms of Palorbitolina
lenticularis
associated with Montseciella arabica
(Fig. 12 )
at the base) and algae (Hensonella, Cylindroporella,
Carpathoporella, Permocalculus). They characterize mid-ramp environments.
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Figure 12:
Thin section photograph. Montseciella arabica
(somewhat oblique transverse section). Kharaib (HST 3) in well No. 21. |
The Kharaib 3 cycle terminates in a discrete erosional surface commonly masked by the stylolites developed at the change in lithologic textures.
Kharaib 4: The cycle consists of a thin TST (7.5 ft) followed by a relatively thick HST (34.5 ft). The transgressive portion is characterized by alternations of grain-dominated packstones and mud-dominated wacke- or pack- stones. Such textural alternations have led to the growth of stylolites. The regressive part, the thickness of which varies considerably from one well to another, displays a net shallowing upward trend. In some cases, marly layers with corals are found toward the top of this cycle. Facies are similar to those found in Kharaib 1 HST or Kharaib 3 HST; they consist of wackestones and mud-dominated packstones with foraminifera (low-spired Trocholina, Chrysalidina, Hensonina and orbitolinids including typical forms of Palorbitolina lenticularis) and algae (Hensonella, Cylindroporella, Carpathoporella, Permocalculus). Environments grade from a mid-ramp setting at the base to an inner- or even innermost- ramp setting near the top.
The top of the Kharaib 4 cycle is marked by a karst surface or by an erosional surface that is commonly masked by stylolites developed in association with the change in texture.
The Hawar Synthem comprises only one cycle and can be recognized easily on the Gamma-Ray log.
The Hawar cycle reflects the flooding of the exposed "Kharaib"
platform. It can be split into a rather thick TST (21.5 ft) and a thin HST (6.5
ft). The transgressive interval consists of a set of thin, shallowing upward
parasequences topped by firm-grounds; the final sequence of the set is
glauconite-rich. At its base is a transgressive lag deposit consisting of a very
thin layer of float- to grain- stones with small lithoclasts reworked from the
underlying unit. It is succeeded by very well sorted fine-grained grainstones,
locally cross-bedded or with features such as keystone vugs, indicative of
foreshore to upper shoreface (coastal) settings. The succeeding dominant facies
is mud-dominated pack- and wacke-stones with abundant orbitolinids (typical and advanced forms of Palorbitolina
lenticularis: Figs. 10
- 11 ); it could be called an
orbitolinid floatstone. These
foraminifera are found associated with Choffatella and Lenticulina. Such an
unusual association suggests reworking in lower shoreface to offshore (outer-ramp) sediments in a storm-dominated setting. The regressive part of the cycle
is represented by a thin shale layer (with some quartz silt) easily identified on
the Neutron Porosity log. At the bottom of this interval, a thin layer of
orbitolinid floatstone with a mudstone to marl matrix indicates condensation.
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Figure 10:
Thin section photograph. Palorbitolina lenticularis (axial section), along with the occurrence of glauconite. Hawar (TST) in well
No. 14. |
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Figure 11:
Thin section photograph. Palorbitolina lenticularis (somewhat oblique axial section), along with
the occurrence of glauconite. Hawar (TST) in well No. 14. |
The top of the Hawar cycle is an irregular (burrowed) surface at the contact between the shale layer below and limestones above. According to our micropaleontological investigations, there is a significant downward shift of facies from an outer-ramp setting below to an innermost ramp setting above.
The Shu'aiba Synthem (51 ft) starts with three thin,
shallowing-upward parasequences. Each parasequence comprises Palorbitolina wackestones at the
base, and microbial boundstones (Bacinella structures, Gakhumella,
coccoid and filamentous structures) with some
algae (Clypeina ummshaifensis Granier 2002, Gyroporella
lukicae Sokač et Velić, Salpingoporella
(Hensonella) dinarica Radoičić) at the top. The remainder of the
unit consists predominantly of mud- and wacke-stones with Cuneolina and rare
Palorbitolina lenticularis, then Choffatella, then Lenticulina and common Epistomina
associated with planktonic foraminifera, including Hedbergella infracretacea (Glaesner).
The uppermost part of the unit (2 ft) is a condensed section. In the reference
well, it consists of two nodular beds with ammonites
(Fig. 13 ). As shown by
microfossil and facies assemblages, most of the unit showed a general deepening
upward, from inner-ramp to outermost ramp and even to a basinal setting.
Sedimentation could not accommodate to ("catch up" with) the relatively
high rate of subsidence. This major change in regional epeirogeny began possibly
at the Hawar - Shu'aiba boundary, or earlier at the Kharaib - Hawar boundary.
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Figure 13:
Photograph of polished core (slab).
Ammonites. Shu'aiba (condensed section = HST) in ADMA well No. 4 of field "B", offshore Abu Dhabi. |
There is no clear evidence of subaerial exposure at the base of the Shu'aiba Formation but there is also no evidence that it was not so exposed. The stacking pattern of the three shallowing-upward parasequences in the lowermost part of the Shu'aiba are retrogradational: the boundstone facies thin progressively upward from one parasequence to the next. This suggests either: - that there was exposure, so that sedimentation records the sole TST in the area studied (the interpretation we favour); - or that there was no exposure and the first shallowing-upward parasequence may represent the LST.
One of us (R.B.) identified Cheloniceras sp., Epicheloniceras sp., Valdedorsella sp., and Gargasiceras sp. that point toward a Middle Aptian (Gargasian) age for the condensed section (HST).
The Bab Synthem (93 ft) is also ammonite-bearing
(Fig. 14 ). Microfossils are sparsely
scattered foraminifera (Choffatella, Lenticulina - Figs. 15
- 16
- and Epistomina).
Palaeontological associations and facies indicate rather deep to shallower
basinal environments. Lithofacies are predominantly organic-rich Nannoconus
oozes - "chalks" - with planktonic foraminifera, including Hedbergella
infracretacea (Glaesner) (Fig. 17 ), and
subordinate mud-dominated fabrics (including Gastropod floatstones).
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Figure 14:
Photograph of polished
core (slab). Ammonites. Bab (TST 1) in well No. 14. |
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Figure 15:
Thin section photograph. Choffatella decipiens (subaxial
section), along with planktonic foraminifera. Bab (LST 1) in well No. 21. |
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Figure 16:
Thin section photograph. Choffatella decipiens (equatorial
section). Bab (LST 1) in well No. 21. |
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Figure 17:
Thin section photograph.
Planktonic foraminifera in an organic-rich Nannoconus
ooze. Bab (LST 1) in well No. 21. |
Chalk facies predominate both at the base and at the top of the interval. On a regional scale, these "sapropelic" deposits were formed in a tongue of the Tethyan ocean bounded by exposed relict Shu'aiba platforms; starvation in lowstand settings favored the deposition and preservation of these organic-rich facies.
One of us (R.B.) identified Cheloniceras sp., Epicheloniceras sp., and Colombiceras sp. These Ammonite occurrences also suggest a Middle Aptian (Gargasian) age for this unit.
In field "A", this uppermost unit of the so-called "Thamama Group" is separated from the overlying formation by a firm-ground at the top of the uppermost limestone bed.
A more precise biostratigraphic dating may be possible based on a new
evaluation of the orbitolinids by one of us (R.S.) that permits a comparison with the
well-known Urgonian limestones of southeastern France and western Switzerland (Charollais et al.,
1992; Clavel et al., 2002; Schroeder et al., 2002).
These fossils suggest
(Fig. 7 ) that:
A significant ecological change takes place at the Lekhwair-Kharaib boundary. The foraminifer Choffatella decipiens in Hauterivian and possibly Early Barremian times inhabited shallow water environments in association with calcareous green algae, but in the Late Barremian and thereafter is found only in deeper environments. This change in habitat may be related to the presence of new competitors, i.e. representatives of the orbitolinids, and the change may be useful in discriminating the two Barremian sub-stages.
Throughout the interval discussed these foraminifera are usually present, though commonly not numerous. However there are several thin layers in which they are particularly abundant. These key beds mark flooding events usually interpreted as storm deposits and are therefore traceable over long distances. On well logs, some of these beds correspond to gamma-ray peaks as in Kharaib 3 TST and Hawar TST. In other cases, as in Kharaib 4 TST, there is no peak on the gamma-ray log but the interval can be detected from Neutron Porosity or Density logs because the slight textural variation associated with it allowed the later development of pressure-solution seams.
The deposition of the Shu'aiba Formation in "A" field of offshore Abu
Dhabi (Fig. 1
) took place under basinal conditions. On the contrary, most onshore fields
in Abu Dhabi (Harris, Hay and Twombley, 1968; Frost, Bliefnick and Harris,
1983),
Qatar and Oman (Witt and Gökdag, 1995) are in shallow-water carbonate platform
settings. But the majority of the existing interpretations of stratigraphic relationships
between onshore and offshore, formations are incorrect. The Bab basinal facies do
not pass laterally into Shu'aiba equivalent platforms with rudists, nor do they
show an onlap or offlap relationship with them. In reality, the Shu'aiba platform facies pass laterally
into
Shu'aiba-equivalent basinal facies; in the same way Bab basinal facies show a
lateral transition into Bab-equivalent platform
facies.
These revisions in correlation (Fig. 2
) are based on data provided by sequence
stratigraphy which, along with new biostratigraphic data, make possible a fresh
comprehensive interpretation of both platform and basin sedimentation during the
time interval in question. It includes three almost complete third order cycles:
Following a forced regression at the end of the Hawar cycle, the Shu'aiba transgression allowed shallow-water carbonates to re-establish in proximal areas. Microbes (Bacinella structures) flourished locally; their growth was sufficient to "keep up" with a rise in relative sea-level in some areas while in slightly deeper areas basinal sedimentation began.
The Shu'aiba HST interval saw the development of various carbonate platforms, either isolated or not, with rudistid colonies developed over some relative highs while in the intra-shelf basin the equivalent section is often condensed.
The older Bab cycle, began with a forced regression. The
Shu'aiba platforms were exposed and karstified. A new generation of
rudist buildups developed either down-stepping from stranded Shu'aiba escarpments
(thus typical "grafted" platforms: Fig. 18 , elsewhere erroneously
termed "Shu'aiba clinoforms" (Fig. 19
): Calavan et al.,
1992; Fitchen, 1997) or on relative highs in the basin
possibly formed by
movement of Palaeozoic salt (Fig. 21
). At this time, intra-shelf basins,
although probably still in communication with the Tethyan ocean, began to become
isolated and starved, thus causing the deposition of organic-rich sediments at the base of
the (older) Bab. Organic content decreased upward with the subsequent rise in
relative sea-level. There were at least two of these intrashelf basins, one
south of the Qatar arch that extended as far as the United Arab Emirates and
reached Oman, and
one north of the Qatar arch that included Bahrain and peripheral portions of Saudi Arabia and Iraq.
|
|
Figure 18:
Seismic section
(flattened on Top Hawar) from onshore Abu Dhabi illustrating the platform
(left) to
basin (right) transition in the Shu'aiba-Bab-Sabsab
interval (S = Shu'aiba; B = Bab). |
|
|
Figure 19:
Distribution of reservoirs (white) and barriers (light grey) in the Bu Hasa field, onshore Abu Dhabi
as interpreted by Harris, Hay and Twombley (1968)
and modified by Hulstrand, Abou Choucha and Al Baker (1985). |
The next cycle, i.e. the older Nahr Umr cycle, also began with a forced regression. Once again platforms of both the Shu'aiba and the (older) Bab were exposed and partially karstified. A third generation of buildups appeared either as downsteps from fossil (older) Bab escarpments, or on relative highs in the basin. It was at this time that the organic-rich sediments near the top of the (younger) Bab were deposited.
Orbitolinid accumulations, a characteristic of the Sabsab facies, formed basinal
onlapping wedges (i.e. healing phase wedges, off-break wedges, or flexure
wedges) on the margins of both the Bab and Shu'aiba platforms (Fig.
6 ), that shed as they
were being drowned by the coeval wide-spread (older) Nahr Umr transgression. The
Sabsab forms a rather thin lag deposit (Fig.
5 )
above the platform facies (either
Shu'aiba or Bab); it may be absent at the edges of the platforms, i.e. in a more
or less narrow by-pass area; at the foot of the platform slopes it commonly
built a rather thick wedge that thinned rapidly basinward as the series became
condensed.
Kennedy and Simmons (1991) reported an ammonite association with Knemiceras in Jebel Madar, Oman, some 50 meters above the base of the Nahr Umr Formation dating it as late Early to early Middle Albian. On the basis of our new ammonite findings the Nahr Umr transgression is not of Early Albian age as stated by previous authors but must be dated as Middle Aptian.
The new
interpretation of the lithologic and faunal succession in the upper part of the
so-called "Thamama Group" in field "A" using allo- and
sequence stratigraphy
(Fig. 7 ) shows that:
This new
stratigraphic model documents explicitly the geometric relations between the
Shu'aiba and the Bab platforms (Figs. 20
- 21
) thus permitting recognition of the significance
of these relationships for petroleum geology with special emphasis on reservoir
geometries and characteristics.
|
|
Figure 20:
Tentative re-interpretation of the stratigraphical relationships
of Fig. 19
|
|
|
Figure 21:
Sketch summarizing the Middle Aptian regional basin history (from Granier
(2000), modified). This figure illustrates the
various platform-basin relationships during the Shu'aiba, Bab and Sabsab times
(A = basin facies; B = organic-rich oozes (Bab LST 1 and 2); C = rudist facies;
D = Bacinella facies build-ups (Shu'aiba TST); E = karst surface; F = Shu'aiba; G = Bab
1; H = Bab 2; I = Sabsab). |
The authors would like to thank ADNOC (Abu Dhabi National Oil Company), ADMA, and Total for permission to publish this paper. We would also like to thank Trevor Burchette and Nestor J. Sander for their thorough and careful review of the manuscript. We have done our best to adopt as many of their suggestions as we found feasible.
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