and phytoplankton biomass in both systems.
Since the width of CB is less than the Rossby radius of deformation (the length scale at which rotational effects become as important as thermohaline processes in determining patterns of circulation), lateral gradients in salinity and density are small relative to gradients along its north–south axis and prevailing flows tend to parallel the main channel. Thus, the primary mechanism of nutrient transport is a two‐layered, gravitational circulation with seaward flow of the surface layer and landward flow of the bottom layer. In contrast, the width of the NAS exceeds the Rossby radius so lateral (east–west) gradients promote the development of basin wide cyclonic gyres (Figure 1.1). Due to river runoff and heating in the late spring and summer and to autumn–winter cooling, gradient currents are established. This geostrophic response leads to a cyclonic gyre, with a NW current flowing into the NAS along the eastern margin and a SW current flowing out of the NAS along the western margin. The former transports warmer and saltier water into the NAS while the latter transports cooler, fresher water out of it. In late fall and winter, the nutrient‐rich Po outflow hugs the Italian coast forming a coastal boundary layer of buoyant water when most of the basin is vertically mixed. As the seasonal pycnocline sets up during spring and summer, the Po outflow tends to spread eastward across the basin resulting in longer residence times of nutrients.
Table 1.1 Mean riverine inputs and physical and ecological characteristics of CB and the NAS
| Riverborne inputs | Po River | Susquehanna River |
| Freshwater input (km3 year−1) | 46 | 36 |
| Total N input (106 kg year−1) | 164 | 63 |
| Mean total P input (106 kg year−1) | 8.8 | 2.8 |
| Mean NOx input (106 kg year−1) | 105 | 43 |
| Mean dissolved inorganic P input (106 kg year−1) | 3.0 | 0.4 |
| Physical characteristics | NAS | CB |
| Length × mean width (km) | 135 × 135 | 320 × 20 |
| Mean depth (m) | 33.5 | 8.4 |
| Surface area (km2) | 18,900 | 6500 |
| Volume (km3) | 635 | 50 |
| Surface area/volume (km−1) | 30 | 130 |
| Dominant circulation pattern | Cyclonic gyres | Partially stratified, estuarine |
| Euphotic zone depth (m) | 10–55 | 3–10 |
| Phytoplankton | NAS | CB |
| Mean surface chlorophyll‐a (μg L−1) | 1.5 | 9.5 |
| Mean phytoplankton production (g C m−2 year−1) | 90 | 450 |
Note: NOx = dissolved nitrate + nitrite.
The parameters of nutrient recycling via pelagic–benthic interactions include net phytoplankton production, deposition of particulate organic matter (POM), benthic respiration, and benthic nutrient regeneration. While phytoplankton production is fivefold higher in CB than in the NAS, benthic community carbon respiration rates are fourfold higher in CB than in the NAS and differences in sediment nitrogen recycling rates (as NH4+) are sevenfold to 15‐fold higher in CB. At the same time, rates of denitrification are nearly identical in the two systems. Thus, when normalized to the rate of respiration, the rate of denitrification (and potential loss of nitrogen to the atmosphere via the release of nitrous oxide and dinitrogen gas) is much higher in the NAS than in CB.
1.2.3. Effects of Nutrient Enrichment
1.2.3.1. Phytoplankton Production
Annual cycles and interannual variability of phytoplankton biomass and primary productivity in CB and the NAS are driven by variations in riverine inputs of buoyancy and nutrients. Differences in circulation patterns and geomorphology are reflected in contrasting patterns and levels of eutrophication. Despite having a much lower annual nutrient load than the NAS, annual phytoplankton production is five times higher in CB than in the NAS. Chesapeake Bay is eutrophic system‐wide while eutrophication in the NAS is confined to the western NAS, which is directly influenced by the Po River. Receiving waters of CB effectively sequester riverborne nutrient inputs into phytoplankton biomass, and efficiently retain and recycle phytoplankton biomass produced in spring (dominated by diatoms) to support high primary productivity during summer. The seasonal accumulation of biomass during spring also fuels the annual occurrence of extensive bottom‐water oxygen depletion during summer in CB. In contrast, seasonal increases in phytoplankton biomass and primary productivity are much lower in the NAS, and bottom‐water oxygen depletion is more sporadic in time and space—patterns that reflect the rapid dilution of riverborne nutrient inputs in the NAS. Dinoflagellate blooms occur most frequently under stratified conditions in both systems. However, in contrast to CB, the formation of large organic aggregates in the NAS (“mare sporco”) during some years displaces the normally frequent dinoflagellate blooms of the summer.
Since 1729, mare sporco following the spring diatom bloom occurred relatively infrequently (1729, 1872, 1880, 1903, 1930, 1949) compared with the late 1970s through the 1990s (1976, 1983, 1988, 1989, 1991, and 1997), perhaps as a consequence of nutrient enrichment, i.e., they tend to occur under high phytoplankton production, fueled by Po River nutrient inputs during spring and summer, leading to the formation of mucus mats that are transported eastward resulting in episodic deposition of POM and the development of isolated patches of bottom‐water anoxia. The location of these mass mortalities varies throughout the season and from year to year, but their cumulative impact results in widespread benthic mortalities in the NAS.
1.2.3.2. Shallow Water Habitats
Like many sublittoral zones worldwide, both systems have experienced dramatic declines in the spatial extent of tidal marshes and submerged aquatic vegetation (seagrass meadows and indigenous macroalgae) as a consequence of cultural eutrophication, coastal development, and sea‐level rise. In this regard, it is noteworthy that relative sea‐level rise (due to both subsidence and eustatic sea‐level rise) is similar in both systems (1.2–8.5 mm
