Crustal Recycling at the Izu-Mariana Margin
There are several reasons why the Izu-Mariana margin (
Fig. 2) is ideal for studying subduction recycling. Significant progress has already been made on many parts of the flux equation. Forearc sites of fluid outflow (serpentine seamounts) have already been drilled (Leg 125; Fryer, 1992), as have most of the sedimentary components being subducted at the Mariana Trench (Leg 129; Lancelot, Larson, et al. 1990). These volcanic arcs and backarcs are among the best characterized of intraoceanic convergent margins, both in space and time (Legs 125 and 126; Gill et al., 1994; Arculus et al., 1995; Elliott et al., 1997; Ikeda and Yuasa, 1989; Stern et al., 1990; Tatsumi et al., 1992; Woodhead and Fraser, 1985), and the problem is simplified here because the upper crust is oceanic, so upper crustal contamination is minimized. Sediment accretion in the forearc is nonexistent (Taylor, 1992), so sediment subduction is complete. Despite the simple oceanic setting and the shared plate margin, there are still clear geochemical differences between the Mariana and Izu Arcs (e.g., in Pb isotopes and elemental enrichments; Figs. 3A and 3B). The divergence of compositions between the volcanics of these two oceanic arcs provides the simplest test for how the composition of the subducting crust affects them. The key missing information is the composition of the incoming crustal sections, particularly the (altered) basement sections.

Existing Crustal Inventory at the Izu-Mariana Margin
Of the eight sites drilled in the seafloor immediately east of the Izu-Bonin Trench (not including the Shatsky Rise sites), only one penetrated basement, Site 197 (Leg 20;
Fig. 2). No sediments, however, and only 1 m of basalt were recovered. Recovery was poor at most of the other sites: less than 25 m of sediment was recovered at all sites drilled during Leg 20 (Sites 194-198), and the recovered material was dominantly pelagic clays above resistant cherts. Although more was recovered at Sites 52 (45 m) and 578 (165 m), drilled during Deep Sea Drilling Project (DSDP) Legs 6 and 86, respectively, coring again was halted by chert layers, leaving hundreds of meters of unsampled sediment below. Prior drilling has provided us with many samples of the upper 50 to 150 m of the pelagic clay and ash unit, but almost nothing of the units below, including the oceanic crust.
* The main goal of Izu-Bonin coring is to sample all sedimentary units and the upper alteration zone (~300 m) of the oceanic crust below.

The success rate in coring sediments and basement to the south, seaward of the Marianas, was just about as poor as that experienced to the north, until Leg 129, when three complete sections (ODP Sites 800-802) were sampled through the cherts to "basement." During Leg 129, sedimentary units were well sampled at Sites 800-802, but normal oceanic crust was sampled at only one site, Hole 801C. At the other two sites, off-axis Cretaceous sills and flows were encountered as "basement." The crustal inventory at the Mariana Trench includes (from top to bottom): pelagic clay, chert, and radiolarite (+ chalk), Cretaceous volcaniclastic turbidites, radiolarite, off-axis Cretaceous intrusives and extrusives, and Jurassic oceanic crust. Leg 129 coring and prior DSDP efforts provided adequate samples of the sedimentary units being subducted at the Mariana Trench (providing estimates of chemical fluxes with better than 30% precision for most elements [Plank and Langmuir, 1998]). However, the only sample of Jurassic oceanic crust, which must comprise the largest mass of crustal material being subducted at the Mariana Trench, comes from the lowest 63 m in Hole 801C (of the ~135 m total penetration into basement in Holes 801B and C, only the lower 63 m of drilling recovered 43 m of normal, Jurassic tholeiitic oceanic crust).
* Thus, the main goal of Mariana coring is to provide a more complete sampling of the upper alteration zones in the Jurassic seafloor, which constitutes a significant part of the budget for many geochemical tracers of the subduction process, including H2O, CO2, Rb, and U.

Existing Crustal Mass Balance for the Marianas
With information in hand, it is possible to calculate many of the input and output fluxes for a few chemical components through the Marianas subduction zone. We consider here a preliminary flux balance for H2O (
Fig. 4). The sediment input is fairly well constrained by previous coring during Leg 129 (Sites 800-802), and by the extensive chemical analyses of the recovered material (Karl et al., 1992; Karpoff, 1992; Lees et al., 1992; France-Lanord et al., 1992) as well as the geochemical logs for the different holes (Pratson et al., 1992; Fisher et al., 1992). As a result, H2O flux estimates for sediments from Sites 800 and 801 are quite consistent with one another (within 15%). The other crustal input flux is the subducting oceanic crust, which is very poorly constrained because of a lack of significant penetration into the mid-ocean ridge (MOR) basement in this area (63 m in Hole 801C). The geochemical budget of elements in the oceanic crust has two sources: primary igneous and secondary alteration. The primary igneous composition is fairly well constrained, based on extensive sampling of modern mid-ocean ridge basalt (MORB) and on the relatively unaltered samples recovered from Hole 801C. The secondary alteration fluxes are virtually unknown, however, and can only be estimated from various other regions, compilations, and assumptions: the average global H2O flux in Peacock (1990), alteration studies of DSDP Hole 504B (Leg 69; Alt et al., 1986) and DSDP Sites 417/418 (Legs 51, 52, and 53; Staudigel et al., 1995), and assuming 10% interpillow material in Hole 801C (Castillo et al., 1992b). These estimates show that the alteration fluxes may be large, but are poorly known. The applicability of existing data (obtained for slow-spreading old crust at Sites 417 and 418 and medium-spreading young crust in Hole 504B) to the crust seaward of the Mariana Trench (old-fast spreading) remains to be seen and is, in fact, a major goal of Leg 185.

Unique to the seafloor seaward of the Mariana Trench is an overprint of Cretaceous basement flows and sills. There are two sources of uncertainty in estimating this flux: the thickness of the Cretaceous "basement" layer and its chemical composition. Calculations based on sonobuoy velocities, reflection data, and drilling results from Leg 129 indicate a 100- to 400-m-thick layer of massive Cretaceous basalt, and possibly some interbedded sediments, overlying Jurassic oceanic crust (Abrams et al., 1993). Although this is not the case for water, the total flux of many elements depends critically on whether this Cretaceous basalt is alkalic (as for Site 800 basalts and various seamounts of the Pigafetta Basin [PB]) or tholeiitic (as for Site 802 basalts of the East Mariana Basin [EMB]). Although plate trajectories (Fig. 2) indicate that the seafloor subducting beneath the Marianas is largely the tholeiitic EMB, we consider both EMB (tholeiitic) and PB (alkalic) type basalts in estimating the water flux into the subduction zone (Fig. 4). Both estimates yield small water input fluxes relative to the sediment and altered Jurassic MORB.

The first measurable outputs from the subduction zone are the forearc fluids, which have shown to be freshened and from a subducted source (Mottl, 1992). It is currently difficult to estimate rates based on the fluid flow itself. We, therefore, use a model based on the total (maximum) water generated during clay mineral breakdown in the subducted sediments (Plank et al., 1994). This calculation is model dependent, but further study of the nature of these fluids will help to identify the actual dehydration reactions that are occurring with depth during subduction. Figure 4 shows that the water outputs to the forearc may be a significant fraction of the sediment input. Magmatic outputs to the volcanic arc and backarc are determined from the chemical composition of arc and backarc basalts (assuming 5.7 and 1.25 wt% H2O above MORB background, respectively; Stolper and Newman, 1994) and from magmatic addition rates. The magmatic arc water flux is the largest of the crustal outputs from the subduction zone.

These preliminary calculations provide some initial insights into the flux balance in subduction zones and reveal where the major uncertainties lie. If we ignore the igneous MORB and Cretaceous basalt contributions as no net gain from the mantle perspective, then the continental water inputs and outputs appear to be remarkably closely balanced across the subduction zone. The balance hinges critically, however, on the magnitude of the basement alteration fluxes. Present estimates are poor, and the actual flux balance could still go either way.
* Drilling through the upper oceanic crust subducting beneath the Marianas can dramatically improve one key flux in the mass balance equation‹the alteration flux.

Existing Crustal Mass Balance for Izu-Bonin
Because neither the sediments nor the altered oceanic crust seaward of the Izu Trench have been sampled to any significant extent, our ability to determine mass balance is much more limited here. However, we can make some predictions about the crustal inputs to the Izu Trench based on the Izu volcanic output. Izu basalts record almost half the K or Ba enrichment of Marianas basalts (
Fig. 3B), whereas sediment mass fluxes into the two trenches are roughly comparable, or even greater, at Izu (600 m of sediment into Izu vs. 400 m into the Mariana Trench). Thus, Izu sediments should be much poorer in K and Ba than Marianas sediments. One way to explain this would be to replace the volcaniclastic sections in the Marianas sediment columns with cherts, which are barren of K and may be very poor in Ba (Karl et al., 1992). This makes some sense given what we know about the history of sedimentation in this part of the ocean‹the Cretaceous overprint east of the Marianas may be absent to the north, east of Izu (Fig. 2), where the seafloor spent a longer time on average beneath equatorial zones of high biologic productivity (Fig. 5), possibly leading to greater sections of chert and/or carbonates. Drilling the seafloor east of Izu can directly test these predictions. Sediment layers are fairly uniform throughout the region, reflecting uniform pelagic sedimentation. Thus, a single hole should give us a fairly representative sampling of sediments being subducted at the Izu Trench. If the extra thickness of sediments off Izu is not dominantly barren cherts, this means that much of this sediment does not contribute to arc magmas, either because it is underplated (we can see that it is not accreted), or because it fails to dewater or melt beneath the arc. Thus, by drilling and sampling the crustal inputs, we can learn more about the process of sediment subduction and recycling.

The geochemical differences between the Marianas and Izu arc volcanics could also be related to the chemical composition of the altered oceanic crust. The K or water contents in the altered basaltic sections may vary regionally, possibly explaining regional variations in K and the extent of melting reflected in Marianas and Izu lavas. This can be tested by drilling the upper oxidative alteration zone, which contains most of the alkali budget in the oceanic crust, in both regions.

Finally, some of the differences between the Izu and Marianas lavas may have nothing to do with subducted input and may be explained by more enriched mantle beneath the Marianas. Evidence for enriched mantle in the region comes from enriched shoshonites at the adjacent volcanic arc (Bloomer et al., 1989; Lin et al., 1989). Although drilling cannot test whether enriched mantle exists beneath the Marianas, it can make invoking it unnecessary.

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