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Geology; March 2009; v. 37; no. 3; p. 203-206; DOI: 10.1130/G25261A.1
© 2009 Geological Society of America
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Deconvolving tectono-climatic signals in deep-marine siliciclastics, Eocene Ainsa basin, Spanish Pyrenees: Seesaw tectonics versus eustasy

Kevin T. Pickering1 and Nicole J. Bayliss1

1 Department of Earth Sciences, University College London, Gower Street, London WC1E 6BT, UK


   ABSTRACT
TOP
 ABSTRACT
INTRODUCTION
 STUDY AREA
 FACIES ASSOCIATIONS AND DEEP...
 TECTONICS VERSUS CLIMATE DRIVERS
 DISCUSSION
 REFERENCES CITED
 
The Eocene deep-marine siliciclastic fill of the Ainsa basin, Spanish Pyrenees, gives unprecedented temporal resolution of the causes and timing of coarse clastic sediment supply to a deep-marine basin. Early Eocene tectonic subsidence linked to Pyrenean orogenesis created the Ainsa basin, with water depths of ~400–800 m above a foundered shallow-marine mixed carbonate and clastic shelf. The ~25 sandbodies or channelized submarine fans in the basin were controlled by the ~400 k.y. Milankovitch frequency, with modes at ~100 k.y. and ~41 k.y. (possibly stacked ~23 k.y.) influencing bottom-water conditions in the basin, causing periodic stratification in the water column across a submarine sill at the western basin margin (early Boltaña anticline). Intrabasinal tectonics defined and controlled the position of eight sandy systems and their constituent fans, in a process of seesaw tectonics, by (1) westward lateral offset stacking of sandy fans due to growth of the eastern side of the basin, represented today by the Mediano anticline, and (2) eastward (orogenward) back stepping of the depositional axis of each sandy system, due to phases of relative uplift of the Boltaña anticline. During basin infill, uplift of the Boltaña anticline led to increasing basin narrowing and depositional confinement. Unlike the earlier depositional systems, the youngest deep-marine system was fed from a more southern sediment source between the growth anticlines, as was the overlying deltaic system. All the older deep-marine sandy systems were fed from southeast point sources, from canyons and erosional lower-slope channels eroding the growing Mediano anticline. The depositional style outlined in this paper might be common to other active margins where siliciclastic basins evolve between active thrusts.


   INTRODUCTION
TOP
 ABSTRACT
 INTRODUCTION
STUDY AREA
 FACIES ASSOCIATIONS AND DEEP...
 TECTONICS VERSUS CLIMATE DRIVERS
 DISCUSSION
 REFERENCES CITED
 
Understanding the interaction between tectonic processes and climate change remains one of the most challenging aspects in stratigraphic analysis in deep time. The principal aim of this paper is to show, using the Eocene deep-marine siliciclastic fill of the Ainsa-Jaca basin, Spanish Pyrenees, that it is possible to gain an insight into the interaction between global climate change and tectonics at a variety of temporal and spatial scales, and therefore constrain the timing and causes of coarse clastic sediment supply. Heard et al. (2008) used ichnological data from the Ainsa-Jaca basin to show that Milankovitch-type processes exerted an important control on deposition in the Ainsa basin. In this paper we integrate the climatic and tectonic data to provide a detailed understanding of depositional processes in the Ainsa basin.


   STUDY AREA
TOP
 ABSTRACT
 INTRODUCTION
 STUDY AREA
FACIES ASSOCIATIONS AND DEEP...
 TECTONICS VERSUS CLIMATE DRIVERS
 DISCUSSION
 REFERENCES CITED
 
The accumulation of ~4 km of Eocene deep-marine siliciclastic sediments in the Ainsa basin, Spanish Pyrenees (Fig. 1), was broadly coeval with maximum rates of tectonic subsidence, shortening, and thrust-front advance in the South Pyrenean foreland basin (Vergés et al., 1995; cf. 2–4 m.y. phases of thrusting in coeval and younger stratigraphic sections by Burbank et al., 1992). The foreland basin evolved with mainly nonmarine and/or marginal marine environments in the east, while farther west there was an overall change from fluviodeltaic to deep-marine systems (Ainsa-Jaca basin), and then distal basin-floor deposits in the Pamplona basin (Mutti et al., 1985). Dating of the Ainsa basin deep-marine deposits suggests that they are middle to late Ypresian and Lutetian (Pickering and Corregidor, 2005; Heard and Pickering, 2008), and overlying deltaic sediments are Bartonian (Dreyer et al., 1999). The deep-marine deposits span ~10 m.y. (time scale of Gradstein et al., 2004), consistent with dating of the more distal deposits in the Jaca-Pamplona basin (Payros et al., 1999).


Figure 01
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  		Figure 1. Location and generalized revised stratigraphy of the Ainsa-Jaca basin (after Das Gupta and Pickering, 2008): TS—turbidite system.

 
This paper focuses on data mainly from the Ainsa basin (Fig. 1). The deep-marine clastics in the Ainsa-Jaca basin (Fig. 21) were fed mainly from a southeast point source, with axial sediment gravity flows toward the northwest in the proximal Ainsa basin (~320°), and more westward across the Boltaña anticline in the relatively distal Jaca basin (~270°) (Pickering and Corregidor, 2005). In the younger, upper Lutetian part of the deep-marine fill in the Jaca basin, west of the Boltaña anticline, an additional northerly-derived sediment supply is recognized (Remacha et al., 1995, 2003). Payros et al. (1997) identified a similar, probably coeval, northerly-sourced submarine channel system in the Pamplona area. The present geographic separation of the Ainsa and Jaca basin deposits, across the Boltaña anticline, prohibits any physical bed correlations, but a detailed sandstone petrographic study has led to a revised correlation of the sandbodies between these basins (Das Gupta and Pickering, 2008; Fig. 1).


Figure 02
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  		Figure 2. Eight sandy systems (>60% sand) are recognized in the deep-marine Ainsa basin, containing 24 sandbodies or channelized submarine fans, that were deposited in various deep-marine settings, which from the oldest are: (1) Fosado (two sandbodies)—lower-slope erosional channels; (2) Los Molinos (three sandbodies)—lower-slope erosional channels; (3) Arro (three sandbodies)—canyon/base-of-slope channel system; (4) Gerbe (two sandbodies)—canyon/lower-slope erosional channels; (5) Banaston (six sandbodies)—base-of-slope erosional channel and proximal basin-floor confined/channel system, but previously interpreted as a canyon system; (6) Ainsa (three sandbodies)—lower-slope erosional channels and proximal basin-floor channelized fans; (7) Morillo (three sandbodies)—base-of-slope erosional channels and proximal basin-floor confined/channel system, but previously interpreted as a canyon system canyon/base-of-slope erosional channel system; and (8) Guaso (two sandbodies)—structurally-confined, low-gradient, clastic ramp. For the Banaston, Ainsa, and Morillo systems, the base-of-slope appears to have coincided broadly with the present-day Rio Cinca and Mediano reservoir.

Map compiled from detailed maps of individual systems with best-fit and, therefore, not accurate for topographic maps or aerial photographs.

 

   FACIES ASSOCIATIONS AND DEEP-MARINE SANDY SYSTEMS
TOP
 ABSTRACT
 INTRODUCTION
 STUDY AREA
 FACIES ASSOCIATIONS AND DEEP...
TECTONICS VERSUS CLIMATE DRIVERS
 DISCUSSION
 REFERENCES CITED
 
The deep-marine sediments of the Ainsa-Jaca basin are described using the facies classification scheme of Pickering et al. (1989). The definition of mass transport complexes is that of Pickering and Corregidor (2005). Seven main facies associations are recognized in the Ainsa basin: (1) channel-axis and/or channel-thalweg deposits, mainly laterally discontinuous, extraformational conglomerates and sandstones (facies classes A, B, C); (2) channel deposits comprising irregularly bedded, thick- and medium-bedded sandstones (facies classes B, C); (3) channel-margin and/or channel off-axis deposits and splay deposits, as mostly laterally discontinuous to irregularly bedded, thin- and medium-bedded sandstones and marlstones (facies classes C, D, B); (4) channel-mouth and/or proximal lobe deposits, as relatively unconfined thick- to thin-bedded sandstones (facies classes C, D); (5) interfan, bedded, sandy marlstone-dominated intervals, commonly with pervasive microfaults (facies classes C, D, E); (6) slope and base-of-slope nonfan deposits, as marlstone-dominated bedded sandy marlstones (including centimeter-scale nummulitic pack-stones) and sediment slides (facies classes F, D, E); and (7) intraformational slope and base-of-slope deposits, as sediment slides and debrisflow deposits containing outsize limestone clasts (facies classes F, A).

A summary of the eight depositional systems is provided in Figure 2 and a schematic depositional model for most of the sandy channelized submarine fans is shown in Figure 3. In general, the base of each sandy channelized submarine fan is defined by a pebbly type II mass transport complex. A predictable, idealized, genetic vertical sequence that tends to fine upward has been proposed using sequence stratigraphic principles, as due to a relative base-level change (Pickering and Corregidor, 2005), probably eustatic sea level. Some of these sequences contain intrasandbody and locally capping (erosive) pebbly type II mass transport complexes, probably reflecting seismically triggered large-scale upper-slope and shelf failure events that are unrelated to any changing relative base level. Lowered base level, however, will tend to favor more widespread upper-slope and shelf mass wastage linked to increased (and erosive) sediment flux to deep water. Thus, the least predictable component of any vertical sequence is the location of type II pebbly mass transport complexes, because they were both seismically triggered and linked to other slope failure processes, and therefore not uniquely associated with changing relative base level. Paleoflow in the southeastern lower-slope erosional channels is generally toward ~290°, compared with the more northern proximal and axial basin floor, where flow was toward ~320°. The widths of the sandy channel fills typically vary between ~0.5 km and 2.5 km, but with the channel-margin heterolithics, levee, and overbank fine-grained and thin-bedded sandy turbidites and marls included, the widths are ~2.5–4 km. It appears that only one channel was active in any sandy fan at any time, probably in the deepest axial part of the basin. Every sandy fan and any channels (typically 10–30 m thick) show a lateral offset stacking toward the west-southwest, away from the east basin slope created by the growing Mediano anticline.


Figure 03
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  		Figure 3. Schematic interpretation of sedimentary environments in sandy systems (e.g., Banastón, Ainsa, and Morillo), in this case, drawn for the Ainsa system. MTC—mass transport complex.

 

   TECTONICS VERSUS CLIMATE DRIVERS
TOP
 ABSTRACT
 INTRODUCTION
 STUDY AREA
 FACIES ASSOCIATIONS AND DEEP...
 TECTONICS VERSUS CLIMATE DRIVERS
DISCUSSION
 REFERENCES CITED
 
The Ainsa basin was bound to the east by the syndepositional Mediano anticline and thrust front associated with the lateral ramp of the Pyrenean thrust units, and to the west by a seafloor high now represented by the Boltaña anticline (Mutti et al., 1985; Dreyer et al., 1999; Pickering and Corregidor, 2005). The sediments within the basin were deformed by both synsedimentary and postdepositional tectonics. The Boltaña anticline broadly coincides with the change from more channelized (Ainsa basin) to less confined, more sheet-like sandy deposits (Jaca basin). Although it is uncertain when the Ainsa basin became a thrust-top basin, it was within the flexural wavelength of the orogenic load and would have responded to the foreland-basin dynamics that drove subsidence. In summary, tectonic and global climatic processes can be matched with specific environmental change in the Ainsa-basin, as follows.

1. The first-order control on basin accommodation for deep-marine sedimentation was tectonic. Subsidence and basin development were driven by Pyrenean orogenesis, with rapid deepening of the basin from a shallow-marine mixed carbonate and clastic shelf to water depths in the range ~400–800 m (Pickering and Corregidor, 2005). The Ainsa basin deep-marine deposits are divided into two distinct successions separated by an angular unconformity, in which the younger unit is both structurally less deformed and displays a west-southwest shift in depositional axis (Pickering and Corregidor, 2005), showing a first-order tectonic control on accommodation and deposition.

Naylor and Sinclair (2007), using a discrete element model approach to analyze the behavior of individual thrust units in the context of asymmetric doubly-vergent thrust wedges (such as the Pyrenees), proposed that the rates of surface uplift, frontal accretion, and exhumation should be punctuated on a time scale linked to thrust-sheet geometry and convergence rates. They concluded that a minimum limit on the time scale of internal (tectonic) variability should be ~4 m.y., consistent with the recognition of a 4–5 m.y. tectonic driver to explain the two successions in the deep-marine Ainsa basin that are separated by an angular unconformity (this study), with the time-averaged driver for the individual sandbodies being an order of magnitude too fast, and therefore better explained by climatic processes.

2. The growth of the ~25 sandy channelized submarine fans in the deep-marine Ainsa basin was controlled by the ~400 k.y. Milankovitch eccentricity frequency, which regulated the voluminous and coarse clastic supply to the basin. The fundamental driver is interpreted to be glacio-eustatic sea-level change associated with the initiation of Antarctic ice sheet growth.

3. Higher-frequency Milankovitch modes, at ~100 k.y. and ~41 k.y. (possibly stacked ~23 k.y.; cf. Raymo et al., 2006), influenced bottom-water conditions in the proximal deep-marine Ainsa basin, causing periodic climate-related stratification in the water column across a submarine sill represented by an early stage in the growth of the Boltaña anticline (Heard et al., 2008). The dominance of eccentricity and obliquity is similar to results from the continental lacustrine Eocene Green River Formation (Machlus et al., 2001). Our age model for the Ainsa basin (~4 km of deep-marine sediments in ~10 m.y.) yields an average sediment accumulation rate of ~40 cm k.y.–1, consistent with that inferred from the spectral analysis (~30 cm k.y.–1) for fine-grained sedimentation (Heard et al., 2008).

4. Intrabasinal tectonics controlled the position of the eight sandy systems and their constituent fans, in a process of seesaw tectonics, by: (1) westward lateral offset stacking of sandy channelized fans due to growth of the eastern side of the basin, represented by the Mediano anticline, and (2) eastward (orogenward) relocation of the depositional axis of each sandy system, due to phases of relative uplift of the Boltaña anticline (Fig. 4). During basin infill, uplift of the Boltaña anticline led to increasing basin narrowing and depositional confinement for the youngest deep-marine Morillo and Guaso sandy systems. Unlike the earlier depositional systems, the youngest deep-marine (Guaso) system was fed from a more southern sediment source between the growth anticlines, as was the overlying Sobrarbe deltaic system. All the older deep-marine sandy systems were fed from a southeast point source, from canyons and erosional lower-slope channels that cut into the growing lateral-ramp zone, including the Mediano anticline. The underlying driver on these tectonic processes must have been controlled by linked and partitioned movement on the thrusts associated with the syndepositional growth of the Mediano and Boltaña anticlines (Bentham et al., 1992). Where outcrop mapping is good, the systems tend to show overall decreasing confinement with age, probably reflecting periods of relative tectonic quiescence after phases of uplift-related movement on the basin-bounding anticlines. Although differential compaction could be invoked to explain at least some of the offset (compensational) stacking pattern for the sandy submarine fans, the consistent westward relocation of successive fans in any system, together with a demonstrable westward progradation of the lower basin-slope sediment entry points between systems, militate against this as a primary driver. Compaction of the marls over the sandy fans, however, would have acted to encourage offset stacking, and therefore would have had some influence.


Figure 04
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  		Figure 4. Summary explanation of evolution of deep-marine sandy systems in the Ainsa basin. Approximate duration of sandy systems is based on ~400 k.y. cyclicity for ~25 sand-bodies and associated fine-grained deposits (channelized submarine fans and interfan deposits) (after Heard et al., 2008).

 

   DISCUSSION
TOP
 ABSTRACT
 INTRODUCTION
 STUDY AREA
 FACIES ASSOCIATIONS AND DEEP...
 TECTONICS VERSUS CLIMATE DRIVERS
 DISCUSSION
REFERENCES CITED
 
The middle Eocene is an important time period for understanding the link between the global deterioration in climate associated with the onset of Antarctic ice development and any possible responses in marine sedimentary systems (e.g., middle Eocene ice; Browning et al., 1997; Miller et al., 2005), but the volume, location, and extent of the ice remain controversial (cf. Edgar et al., 2007; Lear et al., 2008). Ocean Drilling Program Leg 189 data and other stratigraphic records suggest that significant, >10 m, glacio-eustatic changes occurred during the early and middle Eocene ca. 51–42 Ma (Pekar et al., 2005), i.e., coeval with deposition in the Ainsa basin. Following the early Eocene climatic optimum (Zachos et al., 2008), the amplitude of eustatic sea-level change was ~20 m for the early Eocene and ~25–45 m for the middle Eocene (Pekar et al., 2005). These results and conclusions, together with those in Heard et al. (2008), suggest that glacio-eustasy was likely the primary control on sediment flux for the Ainsa basin (cf. Coxall et al., 2005; Burgess et al., 2008).

East of the Ainsa basin, within the fluvial and shallow-marine partial equivalents to the deep-marine deposits (Montanyana Group), the so-called Castissent phase of progradation is within nannoplankton zone NP13, and therefore apparently coincides with a global late Ypresian sea-level fall (Marzo et al., 1988). Mutti et al. (1985) suggested that this fall corresponded with turbidity current deposits fed through a canyon incised in the related shelf edge, i.e., the Charo-Arro system.

In this study, the eight sandy systems are defined on the basis of the consistent westward stacking of their constituent submarine fans, and not the thickness of any intervening marl-rich intervals. The recognition of the systems by Mutti et al. (1985) was based on ill-defined and different criteria, yet for reasons that are not obvious, there remains good overall agreement on the definition of the eight sandy systems and their constituent sandbodies (channelized submarine fans). The thickness of marl-rich sections between the grouped sandy fans in any system is not necessarily greater than that between fans in any system. The eastward stepwise relocation of the basin depositional axis, ~1 km or more, after each sandy system, means that there is a likely associated basin-wide subtle angular unconformity and its correlative conformity.

This study shows the interplay between tectonics and global climate change in a deep-marine basin, at a variety of temporal and spatial scales, thereby providing constraints on the pacing and causes of coarse clastic sediment supply to a deep-marine basin. As in much younger deep-marine siliciclastic turbidite successions at tectonically active plate margins (e.g., Pliocene–Pleistocene of southeastern Japan; Pickering et al., 1999), a glacio-eustatic driver offers the most plausible explanation for the observed changes in deep-marine clastic sedimentation in the Ainsa basin. The depositional style outlined in this paper might be common to other active margins where siliciclastic basins evolve between active thrusts.


   FOOTNOTES
 
Figure 2 is provided as a separate loose insert. Back


   REFERENCES CITED
TOP
 ABSTRACT
 INTRODUCTION
 STUDY AREA
 FACIES ASSOCIATIONS AND DEEP...
 TECTONICS VERSUS CLIMATE DRIVERS
 DISCUSSION
 REFERENCES CITED
 

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Received for publication 8 July 2008

Revised manuscript received 20 October 2008

Manuscript accepted 21 October 2008





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