Hemipelagic deposits on the Mendeleev and northwestern Alpha submarine Ridges in the Arctic Ocean: acoustic stratigraphy, depositional environment and an inter-ridge correlation calibrated by the ACEX results
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- Bruvoll, V., Kristoffersen, Y., Coakley, B.J. et al. Mar Geophys Res (2010) 31: 149. doi:10.1007/s11001-010-9094-9
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The first high resolution multichannel seismic data from the Mendeleev and Alpha Ridges in the Arctic Ocean have been used to investigate the depositional history, and compare acoustic stratigraphies of the three main sub-marine ridges (Mendeleev, Alpha and Lomonosov) in the polar ocean. Acoustic basement on the Mendeleev Ridge is covered by a ~0.6–0.8 s thick sediment drape over highs and up to 1.8 s within grabens. A pronounced angular discordance at 0.18–0.23 s below the seafloor along the middle to upper slopes divides the succession into an upper, undisturbed, uniformly thick, hemipelagic drape (Unit M1) and a partially truncated lower unit (Unit M2) characterized by strong reflection bands. Unit M2 is thicker in intra-ridge grabens and includes three sub-units with abundant debris flows in the uppermost subunit (M2a). The discordance between Units M1 and M2 most likely relates to instability along the middle to upper slopes and mass wasting, triggered by tectonic activity. The scars were further smoothed by bottom current erosion. We observe comparable acoustic stratigraphy and discordant relationships on the investigated northwestern part of Alpha Ridge. Similarly, on the central Lomonosov Ridge, Paleocene and younger sediments sampled by scientific drilling include an uppermost ~0.2 s thick drape overlying, highly reflective deposits with an angular unconformity confined to the upper slope on both sides of the ridge. Sediment instability on the three main ridges was most likely generated by a brief phase of tectonic activity (~14.5–22 Ma), coinciding with enhanced bottom circulation. These events are coeval with the initial opening of the Fram Strait. The age of the oldest sediments above acoustic basement on the Mendeleev- and west-central Alpha Ridges is estimated to be 70–75 Ma.
KeywordsArctic OceanMendeleev and Alpha RidgesDepositional environmentAcoustic stratigraphyPaleocirculationTectonicsInter-ridge correlation
To date, only the Lomonosov Ridge (Fig. 1) has been accessed by modern geophysical surveys and scientific drilling (Jokat et al. 1992; Jokat et al. 1995a; Jokat 2005; Moran et al. 2006). The central part of the ridge is covered by a ~0.5 km thick section of Cenozoic, hemipelagic sediments resting unconformably on a prograding wedge (Jokat et al. 1992; Grantz et al. 2001; Moran et al. 2006). Average Cenozoic sedimentation rates at the drill site were ~1 cm/ka with a major stratigraphic break at 200 m below the seafloor (18.2–44.4 Ma) (Moran et al. 2006; Backman et al. 2008; Sangiorgi et al. 2008)
Hemipelagic deposits which include the upper 0.5 s thick section on the Mendeleev Ridge, northwestern part of Alpha Ridge and the central part of the Lomonosov Ridge in the Arctic Ocean appears to have similar acoustic characteristics, and in particular a disconformity at 0.2 s sub-bottom depth spatially restricted to their respective middle to upper slopes. In this way, parts of the stratigraphic calibration provided by ACEX drilling (Moran et al. 2006) can be put in a wider polar basin perspective.
Outline of the geology, paleogeography and ocean circulation of the Arctic Ocean
Plate tectonic evolution
The submarine Lomonosov Ridge divides the Arctic Ocean into the Amerasia- and Eurasia sub-basins (Fig. 1). Seafloor spreading in a proto-Eurasia Basin was initiated in the early Cenozoic with the opening of the Norwegian Greenland Sea (Karasik Karasik 1968; Talwani and Eldholm 1977; Vogt et al. 1979). Rifting between Greenland and Norway extended into the Arctic Ocean and separated a ~1,700 km long continental sliver from the Barents-Kara Sea margin (Karasik 1968; Vogt et al. 1979). This sliver became the Lomonosov Ridge which subsided below sea level in the earliest Eocene (Moran et al. 2006), but remained shallow until early Miocene (Sangiorgi et al. 2008). Further development of the Eurasia Basin was associated with seafloor spreading along the Gakkel Ridge (Karasik 1968d; Vogt et al. 1979; Eldholm et al. 1990).
Uplift of basement ridges, erosion and subsequent subsidence on the north slope of Alaska and on the Canadian Arctic margin suggest that the Amerasia Basin evolved by rifting and seafloor spreading during Late Jurassic/Early Cretaceous (e.g. Embry 1990; Grantz et al. 1998; Lawver et al. 2002). However, the configuration of the plate boundaries involved remains controversial (Miller et al. 2006) as the geophysical data are ambiguous and plate boundaries difficult to define. The Alpha and Mendeleev Ridge complex is a broad (200–400 km) and up to ~2 km high submarine rise, that extends across the Amerasia Basin from the continental margin north of Canada to the margin of the East Siberian Sea (Fig. 1). The deep area close to 83–84° N, 180° E separates the widest part of the rise, the Alpha Ridge north of Canada, from the narrower Mendeleev Ridge north of Siberia (Fig. 1). The rise constitutes a complex assemblage of alternating high and low standing blocks trending NE–SW at the Mendeleev Ridge (Figs. 1, 2). These structures pass into a series of NE–SW trending grabens and ridges in the western part of the Alpha Ridge and more N–S oriented structures to the east (Fig. 1).
The origin and age of the Mendeleev and Alpha Ridges are unknown and disputed, but most investigators today favour an oceanic plateau (e.g. Van Wagoner and Williamson 1985; Forsyth et al. 1986; Jackson et al. 1986; Weber 1990; Lawver and Muller 1994; Lawver et al. 2002), or a highly attenuated continental crust (Lebedeva-Ivanova et al. 2006; Miller et al. 2006) based on the available data today.
The depositional environment
The Amerasia Basin was essentially land-locked during the Late Cretaceous. The Western Interior Seaway represented a late Albian through middle Maastrichtian shallow connection to the proto-Gulf of Mexico (Kauffman and Caldwell 1993; Sageman and Arthur 1994). A shallow marine connection to the embryonic Eurasia Basin also existed during Turonian through middle Eocene extending from the present Kara- and Laptev Sea via the Turgai area into the present Caspian Sea and the Tethys Ocean (Baraboshkin et al. 2003). Glimpses of the Late Cretaceous/Early Cenozoic paleoenvironment of the Amerasia Basin are represented by short cores from the western part of the Alpha Ridge (Fig. 1). Core 437 from the western part of the ridge contains Campanian-Paleocene biosiliceous oozes representing seasonal upwelling conditions (Dell’Agnese and Clark 1994). CESAR core 6 also includes a biosiliceous unit of Maastrichtian-Paleocene age (Mudie et al. 1986). Black mud of Maastrichtian age in core 533 with a high abundance of amorphous marine matter was probably deposited in a shelf to upper slope environment with high paleoproductivity (Firth and Clark 1998). All cores suggest upwelling conditions during the Mastrichtian into the Paleocene (Kitchell and Clark 1982; Dell’Agnese and Clark 1994; Firth and Clark 1998), and biosiliceous ooze in core 422 may be as young as middle-late Eocene or Oligocene (Bukry 1984; Mudie et al. 1986).
The central flat topped area of the Lomonosov Ridge from 87°30′–88° N has a ~0.5 s, uniformly thick, sediment cover, resting unconformably on dipping strata (Jokat et al. 1992, 1995a). Scientific drilling at this location during the Integrated Ocean Drilling Program (IODP) Expedition 302, the Arctic Coring Expedition (ACEX) (Moran et al. 2006) provides a paleoenvironmental and key stratigraphic tie point. The drilling recovered a 420 m long composite section of Cenozoic sediments comprising three different units: Unit 1—an upper 220 m thick section of glaciomarine clay ranging from middle Eocene to the present including a hiatus (18.2–44.4 Ma); Unit 2—biosiliceous-rich silty clay to ooze (220–318 mbsf) of Middle to early Eocene age; and Unit 3—early Eocene to Middle Palaeocene hard silty clay to mudstone resting unconformably on Late Cretaceous shallow water sands (404.7–427.6 mbsf) (Moran et al. 2006). The unconformity between the Late Cretaceous shallow water sand and Tertiary marine strata was correlated to the angular unconformity LR-3 observed in the seismic reflection data (Jokat et al. 1995a).
Microfossils in the drill cores document an early Eocene Arctic Ocean characterized by a stratified water column (Stein et al. 2006; Stickley et al. 2008) with warm (~18ºC), relatively fresh surface waters (Sluijs et al. 2006; Waddell and Moore 2008) and intermittent connection to the surrounding oceans (Gleason et al. 2009). At the time of the Paleocene-Eocene Thermal Event (~55.5 Ma), a change in the carbon/sulfur ratio, recorded by the occurrence of pyrite and fine lamination in the sediments, indicate euxinic water masses from epipelagic depths (0–200 m) up to the photic zone (Sluijs et al. 2006; Stein et al. 2006). Sediments characteristic of euxinic conditions were recovered from below (subunit 1/6) as well as above (subunit 1/5) the 44.4 Ma–18.2 Ma hiatus and may suggest oxygen deficient conditions throughout that entire interval (Backman and Moran 2009). A return to fully oxygenated conditions is represented by dark brown sediments above the uppermost grey layer dated as younger than 17.5 Ma (Jakobsson et al. 2007). This change to oxygenated conditions has been linked to the opening of the Fram Strait and the establishment of a tele-connection between the water masses of the Arctic Ocean and the North Atlantic (Jakobsson et al. 2007).
The present Arctic Ocean has strong vertical stratification of the water column in its upper part. A well mixed surface layer (20–50 m thick) lies above a region of constant temperature, but increasing salinity to a depth of 150–200 m (Jones 2001). These upper layers isolate the warmer, more saline waters of Atlantic origin below and inhibit melting of the sea ice cover. The oceanic circulation in the present Arctic Ocean is characterized by low kinetic energy and weak cyclonic boundary currents (Rudels et al. 1994; Jones 2001; Woodgate et al. 2007). The boundary current flow (Fig. 1) is predominantly between the 1,500–2,000 m isobaths along the flanks of the Lomonosov Ridge, the Mendeleev Ridge and along the Chukchi Rise (Woodgate et al. 2007). Observed bottom current velocities are <1 cm/s in water depths below 3,000 m and 4–6 cm/s in the 2,000–3,000 m depth range on the south slope of the Mendeleev Ridge (Hunkins et al. 1960, 1969). Water masses in the Eurasia Basin are renewed from the Norwegian-Greenland seas through the Fram Strait gateway, as well as by cold, salty water from the Barents Shelf formed by brine rejection during the formation of sea ice (Aagaard et al. 1985). The Atlantic layer crosses the Lomonosov Ridge into the Canadian Basin from the Siberian continental margin northwards to <88° N at velocities of 1 ~ 5°cm/s (Woodgate et al. 2001). Ventilation of the deep Canada Basin occurs by water spilling over the Lomonosov Ridge threshold from Eurasia Basin (Jones et al. 1995; Jones 2001) and from downslope convection of saltier water formed by cooling and freezing on the shelves (Aagaard et al. 1981, 1985). The time scale for renewal of bottom water in the Canada Basin is ~300–500 years (Aagaard and Carmack 1994; Jones et al. 1995).
The data base and understanding of the present day general circulation pattern and energy level in the Arctic Ocean is increasing. Our knowledge of the paleoenvironment is from seismic studies over Lomonosov Ridge (Jokat et al. 1992, 1995a, and Jokat 2005) and scientific drilling on the central, elevated part of the ridge with recovery of part of the Cenozoic section. The first modern seismic multichannel data from Mendeleev Ridge and northwestern Alpha Ridge (also Jokat 2003) presented here allow us to consider the broader perspective of the central Arctic Ocean paleoenvironment from Late Cretaceous to present.
Data and methods
During 2005, 2,200 km of MCS data were collected in the Amerasia Basin of the Arctic Ocean from the USCG icebreaker Healy, including ~1,100 km over the Mendeleev and Alpha Ridges (Figs. 1, 2). The seismic source consisted of two 4 litre airguns suspended below a depressor plane at the end of an armoured rubber hose. The armoured hose was designed to protect the hydrophone cable and the depressor plane provided a downward force in the turbulent propeller wash. Data were recorded using a 300 m long analogue streamer with up to 24 active channels sampled at 2 ms intervals. The shot interval was 20 s which represented approximately 40 m when the vessel maintained a constant speed of 4 knots (7.5 km/h). During acquisition, the airguns and the front of the seismic cable were frequently forced to the surface by ice blocks and streamer sections were pinched by the random motion of the ice in the wake of the ship. The result was damage to the internal wiring of the cable, loss of recording channels and ultimately loss of entire streamer sections. These problems became more severe as ice conditions worsened; over the western Alpha Ridge only 12 channels remained live.
The seismic data were acquired along crooked ship tracks with the seismic source firing at a constant time interval while the boat speed varied between 0 and 5 knots (0–9.25 km/h). These irregularities were assimilated by a binning procedure (Gjengedal 2004) and the bin size set to 25 m. The data were resampled to 4 ms and dead or very noisy traces removed. The short streamer (300 m) relative to the water depth (1500–4000 m) limited processing options. A simple processing procedure included true amplitude gain recovery, bandpass filter (6-16-80-100), normal move-out correction (NMO), stack, Kirchoff time migration and trace mixing. Interval velocities were obtained from simultaneous sonobuoy measurements.
Breaking ice while acquiring seismic data introduced frequent large amplitude spikes within the frequency band of reflected energy. Noise spikes degrade the data and leads to abundant random “smiles” in the migrated sections. Test processing indicated that the spikes could be significantly dampened with limited consequences to the relative amplitudes by applying a “weak” automatic gain control (AGC window = 1000 ms) before stack. This also gave a better migration result compared to applying AGC post stack. The final processing result was compared to brute stacks, various single channel stacks, as well as data processed without AGC to ensure that none of the reflection characteristics relevant to this study where significantly changed or lost. Deconvolution was not applied to the data because of difficulties in predicting the variable source wavelet, and therefore the processed data are mixed phase. The data are plotted using the Society of Exploration Geophysicists reverse polarity standard, meaning that, for minimum phase data, an increase in acoustic impedance is displayed as a peak on the seismic waveshape (plotted in blue on the figures). All times reported here are two way travel times.
In addition to the Healy 05 (H05) seismic lines from Mendeleev and northwestern Alpha Ridges, a part of the AWI91090 seismic line from the Lomonosov Ridge (Jokat et al. 1992) has also been used in this study. Bathymetric data from IBCAO (International Bathymetric chart of the Arctic Ocean) (Jakobsson et al. 2008) provide the regional morphological context.
Seismic characteristics of the deposits of the Mendeleev and Alpha Ridges
The Mendeleev Ridge
The MU unconformity
Unit M2 rests on acoustic basement and is between 0.4 and 0.6 s thick over the bathymetric highs (Figs 4, 5, 6) and up to ~1.5 s thick in the deepest grabens (Fig 3). Internal reflections are parallel and continuous on the highs where the basement is flat lying or sloping gently, but have a more complex geometry on the slopes and in the grabens (Figs. 4, 5, 7). Unit M2 can be further divided into three subunits based on reflectivity and geometry.
The acoustic image of subunit M2a over basement highs is a 0.10–0.15 s thick well stratified sequence of low impedance contrasts (Figs. 5, 6). Subunit M2a is conformable with the overlying Unit M1 below the crests, but is truncated on the upper flanks of basement highs (Figs. 3, 4, 6). The reflection characteristics and geometry is more complex in grabens and at the margin of the Canada Basin; the subunit is thicker (up to 0.48 s) and a local unconformity is observed and merge upslope with the MU unconformity (Figs. 6, 7, 8a). This local graben unconformity is observed as a strong reflection onlapped by the overlying sediments (Figs. 6, 7). The upper part of subunit M2a includes an interval with convex-up/mounded geometry (Figs 6b, 7) and a transparent to discontinuous signatures (Figs. 6, 7), while the lower part of subunit M2a is dominated by high amplitude reflections.
The top of the unit is marked by a double-cycle reflection (MRB2 at ~0.45–0.55 s below the sea bed) which is well defined below topographic highs and gently dipping slopes, but only locally present at deeper levels within the grabens. The MRB2 reflection band has a wavy signature several places with similar dimensions as observed in M2b (e.g. Figs. 5, 6a, upper panel). Subunit M2c is well stratified and concordant with the acoustic basement on basement highs and gentle slopes (e.g. Figs. 4, 5, 6) but onlaps basement on the steeper slopes and graben walls (e.g. Fig. 4). The contact between subunits M2c and M2b is generally conformable on the highs and gently dipping slopes, but discordant in grabens, where M2c is onlapped by M2b (e.g. Fig. 6). Subunit M2c is about 0.17–0.22 s thick over the topographical highs and 0.25–0.55 s thick in the intra-ridge grabens and lows. Maximum thickness is 0.68 s in the deep grabens between the Chukchi Plateau and Mendeleev Ridge (Fig. 4). A few examples of wedge geometries and weakly tilted sediment packages are present in the lower parts of some grabens (e.g. Figs. 4, 7).
Numerous offsets are present in the acoustic basement and many continue into the sediment section. Fault displacements in the sediment section are similar or less than the corresponding displacements in the acoustic basement. Almost all the faults appear to terminate below Unit M1 at the top of reflective subunit M2b or within Unit M2a (Fig. 3). The wedge shaped geometry observed in subunit M2c (Fig. 7) and weakly dipping sediment packages (Fig. 4) are associated with fault block rotation. Block rotation is also observed where the young part of Unit M2c is onlapping the rotated conformable lower part of the same unit (Fig. 9b).
The northwestern part of the Alpha Ridge
Interpretation of the depositional environment at the Mendeleev and Alpha Ridges
The upper draping units M1 and A1
The sediment cover on the top of the southern Mendeleev Ridge and the western Alpha Ridge show rather similar acoustic reflection patterns and no systematic variation in thickness (~0.65–0.85 s) (Figs. 3, 5, 10, 11a) which suggests broadly similar depositional environments. The upper Unit M1 forms a completely undisturbed drape (0.18–0.23 s thick) over both high and low areas across the entire Mendeleev Ridge. The elevated ridge has been isolated from terrigenous input except for the suspended clay-fraction carried within the bottom nepheloid layer (Hunkins et al. 1969), and Unit M1 is interpreted to be a hemipelagic deposit. The thickness and acoustic characteristics of the upper Unit A1 on the north flank of the western Alpha Ridge are comparable to the observations of Unit M1 from the Mendeleev Ridge (Figs. 5, 11a), and Unit A1 is similarly considered a hemipelagic deposit.
The uniform thickness and absence of any pronounced reflector pinch-out/erosion suggests that the bottom circulation was sluggish, potentially similar to the present day bottom current velocities of 4–6 cm/s (Hunkins et al. 1969).
The nature of the MU- and AU unconformities
The discordance between Unit M1 and Unit M2 (the MU unconformity) along the middle to upper slopes of bathymetric highs on the Mendeleev Ridge represents truncation of laterally uniform internal layering in Unit M2 and varies between a smooth surface, a irregular transition and a staircase block pattern at various scales. Post-depositional removal of sediments is indicated by abrupt truncations rather than by tapered internal layers (except one locality at the bottom of Unit M1 and in subunit M2a, Fig. 6a, upper panel). Other evidence of sediment removal is the local incisions in Unit M2 on the eastern slope of Mendeleev Ridge and the small mounds which probably represent erosional remanents (Fig. 8). On the northwestern Alpha Ridge, sediment disturbance in the crestal areas obscure the contact between units A1 and A2 (Figs. 10, 11b), but Unit A2 is truncated on the north flank of the ridge (the AU unconformity) in a similar manner as Unit M2 on the Mendeleev Ridge (Figs. 10, 12).
Removal of sediments may result from either mass wasting event(s) on unstable slopes or from bottom current erosion over time. Local undercutting of slopes by bottom current erosion, the presence of gas/gas hydrates (e.g. Nixon and Grozic 2006; Esmerode et al. 2008) or loading events such as earthquakes, tides or sea level changes can all trigger slope instability. Failed sediments can produce a surface of progressively disintegrated blocks (Kvalstad et al. 2005), a process critically dependent on the degree of strain softening after failure (Gauer et al. 2005). On the Mendeleev Ridge the chaotic to staircase blocky pattern of the disconformity at the slopes affecting very limited part of the sediment succession in depth, aswell as the locally rough incised appearance suggests sediment removal by local mass wasting events. Evidence of related deposits is evident within the upper part of the underlying Unit M2 within grabens, particularly the upper subunit M2a (Figs. 4, 6, 7, 8)
Unit M2 on the Mendeleev Ridge forms a uniform, 0.4–0.6 s thick, drape over acoustic basement highs, and thickens to 0.8–1.4 s in intervening grabens. The complex stratigraphies in the grabens mostly represent infill of bathymetric lows (e.g. Figs. 4, 6). Up-slope onlap from rapid infill is particular pronounced in the uppermost subunit M2a. Subunit M2a are characterized by discontinuous to continuous reflections grading upwards into a more transparent acoustic signature (Figs. 6, 7). The discontinuous reflection patterns are interpreted as debris from proximal larger mass wasting episodes where internal layering was partly destroyed (e.g. Mitchum et al. 1977; Fiedler and Faleide 1996; Kuvaas and Kristoffersen 1996; Nygard et al. 2005). Transparent or weakly reflective intervals may have resulted from subsequent hemipelagic input and more distal turbidites originating from multiple smaller mass wasting events (e.g., Larter and Cunningham 1993). The input of debris appears to have increased after the deposition of subunit M2b. Normal faults flanking basement highs on the Mendeleev Ridge all terminate below Unit M1 i.e. high in subunit M2b or within subunit M2a (Figs. 3). Stratigraphic offsets in the sediment succession which are less than the corresponding offsets in the acoustic basement levels suggest both faulting and reactivation of older basement faults. Tectonic activity may have triggered the mass wasting, and the relative abundance of debris in subunit M2a in grabens suggests a tectonic episode at the time of deposition of this subunit. The incised unconformity surface between subunits M2a and M2b observed along the northern slope of the Mendeleev Ridge (Fig. 8) may also relate to mass wasting triggered during this interval.
The predominance of smooth truncations of intact layering and no observations of remanent slide scar head walls at the perimeter of basement highs (the MU unconformity) suggest that temporal and spatially limited erosion/non-deposition associated with bottom currents have been important. Gradients in geostrophic, contour-following bottom currents attenuate sediment deposition or erode at the perimeter of a ridge crest and redistribute sediments into contourite drifts (Faugères et al. 1999; Stow et al. 2002). However, the volumes of redistributed sediment would be relatively small in this case. Indications of current activity in the Amerasia Basin is seen from the convex-up sediment body in a graben on the Lomonosov Ridge close to Makarov Basin (Fig. 8 of Jokat (2005), shot point 1600–1400) and possible current erosion on the north slope of the Alpha Ridge (Jokat 2003). Onlap and slight convex up patterns in the upper part of subunit M2a may also represent contourite deposits (Fig 6b, 7). Sediment drift deposits interbedded with mass waste products are difficult to recognize (Faugères et al. 1999; Stow et al. 2002). We suggest that the combined effect of a tectonic episode and bottom current activity both contributed to slope instability and removal of sediments from the upper slopes of basement highs on the Mendeleev Ridge. Similarities in the signature and stratigraphic level of the main AU unconformity at the northwestern Alpha Ridge suggest a similar and coeval process including the north western Alpha Ridge.
The reflection bands and their implications for the depositional environment
Unit M2 on the Mendeleev Ridge and Unit A2 on the northwestern Alpha Ridge are interpreted as hemipelagic deposits, and both include several large amplitude, multi-cycle reflections. Acoustic impedance contrasts within hemipelagic sediments are primarily generated from saturated bulk density contrasts due to variations in the clay content of the sediment. The biogenic carbonate and siliceous components show relatively small velocity contrasts (Mayer 1980; Bayer and Ott 1983). Where multiple thin layers are present, acoustic tuning effects may also be an important cause of strong reflections. Silica-rich sediments are abundant in the Paleogene and older sediments recovered in short cores from Alpha Ridge (Mudie et al. 1986), and strong reflections can also be produced by diagenetic fronts such as opal-A to opal-CT transition (Hesse 1990; Guerin and Goldberg 1996). The acoustic response is a bottom simulating reflection of moderate to high amplitude and positive polarity (Hein et al. 1978; Davies and Cartwright 2002) that may cross-cut depositional surfaces (Davies and Cartwright 2002; Meadows and Davies 2007).
The top of the lower double-cycle reflection bands (MRB2 and ARB3) on the Mendeleev and northwestern Alpha Ridges appears to be a positive amplitude reflection with a seismic signature similar to the planar diagenetic front described by Davies and Cartwright (2002) and Meadows and Davies (2007). The lower reflection bands (MRB2 and ARB3) have constant amplitude, show no cross-cutting relationships, and MR2B is present in grabens where it is much deeper buried. At this point we are unable to discriminate between alternatives where the lower reflection bands may represent a change from bio-siliceous sediment to clay dominated lithology or represent a diagenetic front within a silica-rich interval.
Basement topography and faulting
The difference in sediment thickness of the lowermost interval M2c between the grabens and surrounding highs on the Mendeleev Ridge suggests ridge relief was in part established prior to deposition of this lowermost unit. Several basement faults predate sediment deposition or have larger basement level offsets than offsets higher in the sediment cover (Fig. 3). Local syn-depositional fault growth is documented by local wedge geometries in subunit M2c and basal sediments rotated with a large fault block also indicate basement uplift early in this interval (Fig. 9b). Topographic relief was further enhanced at the time of deposition of sub-units M2b and M2a although there is no evidence for growth wedges suggesting that the extensional tectonic movements were episodic. The area along the north eastern slope of Mendeleev Ridge characterized by a chaotic and transparent acoustic pattern extending to the top of subunit M2b (Fig. 9a) and disturbing the sediment continuity around them, may represent an intrusive event contemporaneous with the tectonic episode which destabilized sediments on the slopes of basement highs and generated the MU discontinuity. Alternatively the diffuse reflections may be due to gas blanking.
The data coverage of the Alpha Ridge is limited, but offsets in basement levels seem to be pre-depositional in areas with undisturbed acoustic stratification (Fig. 11a). However, faults are abundant where the stratigraphy is disrupted (Fig. 11b), but the age of this disturbance can not be constrained and may be recent (Kristoffersen et al. 2009).
Stratigraphic correlation between the Mendeleev, northwestern Alpha Ridges and the Lomonosov Ridge
Mendeleev and northwestern Alpha Ridges
Seismic stratigraphy and core seismic integration at the ACEX drill site, central Lomonosov Ridge
The LU unconformity appears as a smooth surface in its upper part, passing down-slope into a series of progressively disintegrating fault blocks (Fig. 15, lower panel right) where intact strata have become unstable and partly removed by mass wasting. No relict head walls are apparent and the remaining sediment scar has been smoothed. The LU unconformity on Lomonosov Ridge appears restricted to the flank as on Mendeleev and Alpha Ridges and may have been generated from sediment instability induced by slope undercutting from bottom currents an/or tectonic movements. The presence of sediment drift deposits farther down the Eurasia flank along the same AWI09091 seismic line (Fig. 2 in Jokat et al. 1992) support bottom current activity in this interval.
The acoustic stratigraphic level associated with the LU unconformity projects to the approximate position of the subunit 1/4–1/3 boundary (~14.5 Ma) at the ACEX drill site (Fig. 16) using results of the core-seismic integration of Backman et al. (2008). Alternatively, a match between the seismostratigraphic position of the LU unconformity and the core hiatus would be more appropriate. Below the hiatus, these authors correlate the boundary between subunit 1/6 and Unit 2 to the lower part of the double-cycle reflection band (Fig. 16), and the boundary between Unit 2 and -3 to the top of the second reflection band (Jakobsson et al. 2007; Backman et al. 2008).
An inter-ridge stratigraphic correlation
an upper ~0.20–0.25 s thick draping unit that is conformable with underlying strata over flat or gently sloping ridge highs, but rests on truncated layers on the adjacent upper slopes (Figs. 3, 10, 14), and
sediments below the upper drape also have the character of hemi-pelagic deposits and include several high amplitude, multi-cycle reflection bands
The water column over all of the ridge crests would have shared the same, post-early Eocene surface water properties, but differed at depth due to different bathymetric thresholds in the deeper restricted sub-basins. Lomonosov Ridge has a more recent subsidence history and was closer to the margin of the early Cenozoic polar basin. The upper uniform sediment drape on the Mendeleev-, northwestern Alpha and Lomonosov Ridges suggests that units M1, A1 and L1 are of similar lithology and time equivalent with a basal age of late early Miocene (~14.5 Ma) (Fig. 16). Discordant surfaces on the flanks of the Mendeleev Ridge and northwestern part of Alpha Ridge are most likely the result of tectonically triggered slope instabilities and mass wasting at a time also associated with erosive bottom currents. The nature and stratigraphic position of the LU unconformity below the flanks of the central Lomonosov Ridge are similar and considered to relate to the same phase of tectonic and bottom current activity.
Any attempts at inter-ridge correlation of the pre-early Miocene strata (Fig. 16) will require two possible alternatives since a hiatus (18.2–44.4 Ma) is associated with the top of the upper reflection band on the Lomonosov Ridge (Jakobsson et al. 2007; Backman et al. 2008)
Model 1: A direct correlation between reflection bands (Fig. 16, Mod. 1) will imply reduced deposition, non deposition or erosion on the Mendeleev Ridge and northwestern part of Alpha Ridge as documented for the central part of the Lomonosov Ridge (Moran et al. 2006; Sangiorgi et al. 2008).
Model 2: Assumes continuous deposition on the undisturbed crestal areas of the Mendeleev and Alpha Ridges during the hiatus on the Lomonosov Ridge at the ACEX drill site. The lower Unit L2 on the Lomonosov Ridge is capped by a middle Eocene early Miocene stratigraphic break and the initial vertical extent of the upper reflection band is unknown. We therefore correlate the base of the upper reflection band on the Lomonosov Ridge with the bases of bands ARB2 and MRB1 on the Alpha and Mendeleev Ridges, respectively (Fig. 16, Mod 2.). Deeper in the succession, the top of the lower reflection band at the Lomonosov Ridge has been correlated with bands ARB3 and MRB2.
The second alternative is favoured because; (1) the ridge flank unconformities have associated correlative surfaces over the ridge highs with no related impedance contrasts, and (2) a condensed or truncated section on the highs of Mendeleev Ridge is less likely as subunit M2b has approximately the same thickness and signature within the grabens as below the highs.
Origin of the MU, LU and AU unconformity surfaces at the Mendeleev Ridge, northwestern part of Alpha Ridge and Lomonosov Ridge
The disconformity topographically restricted to the upper and middle slopes of Mendeleev Ridge and northwestern part of Alpha Ridge and Lomonosov Ridge is suggested to originate from mass wasting induced by tectonic events and the action of enhanced bottom currents. Debris from mass wasting is particularly abundant in adjacent grabens within subunit M2a right below the discordance, while evidence of sediment drifts in the same stratigraphic position is more subtle. Smooth truncations of intact layering dominate and no evidence of relict head walls left from displaced sediments suggests bottom current erosion. Offsets in acoustic basement and the sediment cover appear to vanish within or below subunit M2a and the relative abundance of debris flows within grabens suggest slope destabilization culminated during deposition of subunit M2a. A chaotic reflection pattern along the eastern slope of Mendeleev Ridge (Fig. 9a) could be interpreted as local igneous activity within this period. The phase of tectonic activity is estimated to early Miocene (~22–14 Ma), assuming continuous deposition at an average Neogene sedimentation rate of 1.2 cm/ka (Backman and Moran 2009) and average compressional velocity of 1.6 km/s.
The Mendeleev and Alpha Ridges are distant from known Oligocene/early Miocene plate boundaries or zones of tectonic activity such as (a) the Gakkel spreading centre and its continuation as an extensional regime on the Laptev Sea continental margin (Sekretov 2001 Drachev et al. 1998), (b) the proposed crustal shortening north of Greenland (Brozena et al. 2003) and (c) the main phase of folding and thrusting during the Eurekan orogeny (De Paor et al. 1989); the two last events being no younger than Oligocene. Possible trajectories of transmitted far-field effects from tectonic events are difficult to document as there is no reported significant sediment deformation in the Eurasia Basin (Jokat et al. 1995b; Jokat and Micksch 2004), in the Makarov Basin (Sorokin et al. 1999), or in the central Canada Basin (Grantz et al. 2009). The central part of Lomonosov Ridge started subsiding in the early Miocene, 35 million years after separation from the Barents- and Kara Sea margin (Sangiorgi et al. 2008), but how this delay relates to regional plate stresses remains highly speculative (O’Reagan et al. 2008). We feel there is insufficient data at present to establish a direct link between the observed early Miocene episode of extensional tectonics on Mendeleev Ridge and regional tectonic events. Another possibility is a regionally restricted activity in the central Arctic Ocean akind to documented intra-plate local events of faulting and doming occurring from Late Eocene to Late Miocene along the northwest European Atlantic continental margin (Doré et al. 1999).
Bottom current erosion has most likely contributed to generate smooth unconformable surfaces between units M1 and M2 on Mendeleev Ridge and A1 and A2 on northwestern Alpha Ridge, Lomonosov Ridge, respectively as well as destabilized the slopes. However, the internal circulation below the wind-driven surface layer (0–200 m) in a closed ocean basin is primarily induced through diapychnal flow from lateral differences in vertical mixing. This process would have been suppressed in the stably stratified water masses (Stein et al. 2006; Stickley et al. 2008) of a euxinic (Sluijs et al. 2006; Stein et al. 2006) pre-early Miocene Arctic Ocean. The Late Cretaceous- early Cenozoic bottom currents in the Amerasia Basin were probably slow while only shallow seaways existed as there is no evidence in the seismic reflection data from Alpha and Mendeleev Ridges of extensive bottom current erosion within the lower units A2 and M2, respectively. Also, the uppermost Paleocene to middle Eocene sequence on Lomonosov Ridge suggests sluggish deep water circulation (Brinkhuis et al. 2006).
The change represented by early Miocene opening of the Fram Strait gateway (Engen et al. 2008) provided a tele-connection to the North Atlantic thermohaline circulation, primed Arctic Ocean circulation and oxygenated the basins (Jakobsson et al. 2007). Opening of the Fram Strait and exchange of deepwater between the Arctic and Atlantic Oceans is also suggested to relate to an Early Neogene massive increase in contourite drift formation in the Northern Atlantic and Norwegian-Greenland Sea (Laberg et al. 2005).
Enhanced current circulation may have started with the transition to an oxygenated Arctic Ocean at about 17.5 Ma (Jakobsson et al. 2007) and lasted until the onset of deposition of the undisturbed upper drape (Unit L1) correlated to subunit 1/4–1/3 boundary in the ACEX core (~14.5 Ma). The omnipresent uniformity of the upper drape (units M1, A1 and L1) suggest relatively slow post middle Miocene bottom current circulation much like today (Hunkins et al. 1969; Woodgate et al. 2001; Isachsen et al. 2003; Woodgate et al. 2007).
Implications of an inter-ridge stratigraphic correlation
The implications of Model 2 (Fig. 16) are continuous deposition over the basement highs while the unconformities between units, MU on Mendeleev Ridge, AU on northwestern Alpha Ridge and LU on central Lomonosov Ridge, formed along their respective upper flanks. Sediments of subunit M2b on the Mendeleev Ridge and subunit A2b on northwestern Alpha Ridge may be equivalent to the Eocene biosiliceous clays and mudstones (ACEX Unit 2) deposited from 49.7 Ma and onwards. Biosiliceous ooze of this age is recovered on Alpha Ridge in core 422 (Bukry 1984; Mudie et al. 1986). A biosiliceous-rich unit would be poorly consolidated and susceptible to slope failure as observed in more recent events on Lomonosov Ridge (Kristoffersen et al. 2007). Model 2 also implies that the top of reflection bands MRB2 and AR3B are equivalent to the top of early Eocene and older silty clays and mudstones (49.7 Ma) (Fig. 16). However, the latter correlation is of questionable value as the late Paleocene- early Eocene depositional environment on the shallow Lomonosov Ridge most likely differed from the older and deeper Mendeleev and Alpha Ridges. Also the thermal and subsidence history of Lomonosov Ridge are different from Mendeleev and Alpha Ridges and leave open any associations of the lower reflection bands on Mendeleev and Alpha Ridges with Opal A to Opal CT transition as suggested for Unit 2/3 transition in the ACEX core from Lomonosov Ridge (O’Reagan et al. 2009). The age of the oldest sediments above acoustic basement on the Mendeleev and northwestern Alpha Ridges is estimated to be ~70–75 Ma from the thickness (~0.20–0.25 s) below the top of MRB2 and ARB3 (Fig. 13) assuming a seismic interval velocity of 2.0 km/s and a hemipelagic sedimentation rate of ~1 cm/ka.
Summary and conclusions
The top of Mendeleev Ridge and northwestern part of Alpha Ridge are draped by a 0.6–0.8 s thick succession of hemipelagic sediments above acoustic basement. The lack of systematic variation in thickness and rather similar acoustic reflection patterns argue for broadly similar depositional environments on the two ridges.
An angular discordance confined to the middle and upper slopes of the bathymetric highs is well documented on the Mendeleev Ridge (the MU unconformity), and also observed on the investigated northwestern part of Alpha Ridge (the AU unconformity). This disconformity divides the section into; an upper, uniform and undisturbed drape, and a lower unit characterized by internal strong multi-cycle reflection bands. Debris from mass wasting is abundant in intra-ridge grabens on Mendeleev Ridge below the stratigraphic level corresponding to the MU unconformity. The angular discordance is suggested to result from the combined effect of sediment instability and mass wasting triggered by tectonic activity and smoothed by enhanced erosive bottom currents acting at the same time. Opening of the Fram Strait gateway and increased efficiency of an oceanographic circulation may explain enhanced bottom currents within the estimated ~22–14 Ma time frame for deposition of subunit M2a on Mendeleev Ridge, but any direct link between normal faulting on the Mendeleev and Alpha Ridges and regional plate stresses remains elusive.
The upper 0.5 s of the sediment cover on the Mendeleev and northwestern Alpha Ridges share common attributes with the central part of the Lomonosov Ridge. We make a correlation between the MU unconformity on the Mendeleev Ridge and the AU unconformity on Alpha Ridge to an unconformity on the flanks of central Lomonosov Ridge (the LU unconformity) stratigraphically above the hiatus at the ACEX drill site (18.2–44.4 Ma). Calibration to the ACEX results suggests a period of increased bottom current activity in the Arctic Ocean (Fig. 16) starting at the transition from euxinic to oxic conditions at the ACEX site (17.5 Ma) and becoming less effective at the beginning of deposition of Unit M1 (14.5 Ma). The 0.2 s thick drape (units L1, A1 and M1) above the flank disconformity on all three ridges is represented by hemipelagic clays of glaciomarine origin deposited in a low energy regime similar to the present day conditions. Sediment deposition on basement highs on all ridges was most likely continuous throughout the phase of mass wasting and bottom current erosion along their respective flanks.
The lower unit on Mendeleev (M2), northwestern part of Alpha (A2) and Lomonosov (L2) Ridges is dominated by internal strong multi-cycle acoustic reflection bands. Two alternative inter-ridge correlations follows from the hiatus recorded at the ACEX drill site. The preferred alternative implies continuous deposition on the highs of the Mendeleev and Alpha Ridges while non-deposition or erosion occurred on the crest of central Lomonosov Ridge. The correlation implies that the acoustic reflection bands on the Mendeleev and northwestern Alpha and ridges most likely relates to changes from clay rich deposits to bio-siliceous sediment and back to clay dominated lithology again.
We thank captain D. Oliver and the crew of the USCG icebreaker Healy. Healy cruise 0503 by NSF award # 0449898 to Geophysical Institute, University of Alaska, Fairbanks, and # 0447440 to Texas A&M University, College Station, Texas. MCS acquisition and Norwegian participation in Healy cruise 0503 was funded by the Norwegian Petroleum Directorate. We are grateful to the Healy (2005) Seismic Team (Paul Henkart, Scripps Institution of Oceanography, USA; Tore Arthun, Hans Berge and Erik Grindvoll, University of Bergen, Norway; Hedda Breien, University of Oslo, Norway; Dayton Dove, University of Alaska, Fairbanks, USA; Nina Ivanova, University of Uppsala, Sweden; Fredrik Ludvigsen, Thor Heyerdahl High School, Larvik, Norway; and Karina Monsen, Alta High School, Alta Norway) for their effort and companionship during the cruise. We also thank two anonymous reviewers for their efforts and constructive comments.
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