A Short Term Mineral Fluid Exchange

A system is Material moving most stable when it has reached equilibrium. A out of the cell system will tend to go to equilibrium (lowest, accessible energy state) in the absence of added energy (Figure 2).

Bradbury’s (1967) dissertation research was the first comprehensive study of Zuni Salt Lake maar. Based on a radiocarbon age of 22.9 ± 1.4 ka 14C yr BP (Haynes et al., 1967) on aquatic, calcareous algae from Zuni Salt Lake lacustrine deposits 15 m above the present lake level, he concluded that the Zuni Salt Lake maar formed during the late Pleistocene. This single date provided a maximum age for the Zuni Salt Lake maar but has long been viewed as suspect because of probable hardwater carbon-reservoir effects. Subsequent argon dating of Zuni Salt Lake volcanic rocks resulted in low-resolution plateau ages of 114 ± 38 ka and 86 ± 31 ka (McIntosh and Cather, 1994).

Only one method of planktonic sampling was used so comparison with another method of sampling cannot be done. It is safe to assume that the most appropriate method of sampling in these areas was previously determined by the lab instructor. Isolation of organisms in the samples was met with some difficulty as there was very little life to be observed. Once isolated however, a general identification was simple with the use of the “quick picks” section of the Marine Invertebrate Zoology Lab Manual. One particular organism isolated from the “T-docks” samples, a foraminiferida, was chosen for scientific drawing (Figure 1).

Scientist in order to measure the depth of the ocean use “Bomb Sounding” this is where they throw TNT into trenches and from the echo that it gives the scientist than approximate its depth. “Recent expeditions such as the HADES project in the Pacific suggest that fish are not found below 27,560 feet. But the hadal zone extends to 36,000 feet”, (Cock-Starkey 9). The development of the “DeepSea Challenger” allowed the ability for scientist to travel down the trench to collect rocks, sediments,and biological samples. Scientist from Scripps Institute Oceanography, University of Hawai’i, and Jet Propulsion Laboratory all joined in into the DeepSea Challenger setting their research on marine biology, microbiology, astrobiology, marine geology and geophysics. Living in the deepest part of ocean surfaced thoughts of marine life being non-existent because of the lethal conditions it has , but past findings of marine life as deep as 27,560 feet shook scientist. Marine adaptation has grown because of the frequent findings of marine life such as the following: Frilled Shark (5,000 ft), Giant Spider Crab (estimate 1,000 ft), Atlantic Wolffish Pair (1,600 ft), Fangtooth Fish (16,500 ft), Six-Gill Shark (8,200 ft) and etc. All these deep sea creatures have adapted to low oxygen levels and the lightless depth of the

The Sublittoral is the region of the ocean below the low tide limit and extends all the way to the edge of the continental shelf. This zone is submerged permanently despite the turn of the tides and the intra/interspecific competition for space is extreme. Organisms in this region rarely experience intense sun or air exposure and organisms such as blue

<b>Introduction</b><br>Think of a world which existed 290 million years ago. As you look out over the terane in front of you, you think that you are on an alien planet. You see volcanoes spewing ash and lava. Beside them is the ocean which is swarming with many different species of echinoderms, bryozoans and brachiopods. As you look down onto the sea floor you are amazed at the countless number of starfish and urchins. Some animals leave you can't even describe and you have no idea even what phylum they belong to. This is a world at its height in diversity of oceanic species. Millions of wonderous species existed at this time in the ocean and most of them will never appear again in earth's history. In the geologic time scale, a million

The Crato Formation lithologies were most likely deposited when there was a marine transgression; which is what the Cretaceous period is renowned for (Hu et al. 2012). The build-up of laminated limestones and different lithologies in the stratigraphic column could suggest that it was a lagoon depositional environment (Martill and Frey, 1998).

British Colombia in Canada, much like California in the United States, used to be a shallow sea and home to much sea life and is now home to thousands of marine animal fossils. For this reason it is believed that Dinosaur Provincial Park consisted of a lot of sands and muds that are characteristic of costal plains (Sues, Henderson, & Tanke, 2010, pg. 1292). When Sues, Henderson, and Tanke (2010) where going about measuring fossil shifts and the amount of fossils that have been lost they took into account the amount of soil that erodes away every year, the vertical and horizontal distribution fossils found within the park, and large landmarks such as rivers and glaciers that could effect fossils in the area (pg.1293). Accounting for these factors

The base of IIIb1 appears slightly oxidized and yielded an age of 2277± 36 14C yr BP. Above this is a ~60-cm-thick, organic-rich “black mat” (IIIb2) consisting of multiple thin beds containing varying amounts of plant matter including both decomposed humic material and uncharred plant macrofossils that constitute a significant proportion of the sediment volume in the most organic-rich deposits. The IIIb2 black mat was formed between 1934 ± 29 14C yr BP and 1759 ± 25 14C yr BP, with the most organic-rich portion predating 1833 ± 36 14C yr BP. Organic carbon content of the black mat varies, but the highest values are ~2%. Plant remains in IIIb2, consisting mostly of bulrush achenes and pollen, indicate emergent aquatic floodplain vegetation, and the unidentifiable stem fragments ubiquitous throughout the layer are likely also bulrush (Figure 8). Faunal remains within IIIb2 at 11-37 include snail and ostracode species indicative of marshy conditions (Table 4). From the base of IIIb1 to the sharp upper boundary of the IIIb2 black mat, a trend of decreasing calcium carbonate, increasing gypsum, and increasing organic carbon is evident. Gypsum content ranged from 3.7–16.6% and occurred as tiny clumps of intergrown lathe crystals, whereas carbonate content ranged from ~4–13% and occurred as small soft

The fossils in the lower silty layers were most likely formed below water by normal geological processes. The sea level rose covering the organisms and the layers of silt settled above them. In the upper sandy layers the fossils could have been formed above water by a sudden catastrophic event as a result of ongoing erosive processes. The conditions in which the fossils formed were likely a result of wave action which eroded the coast line until it was unstable. When the sea level receded there was a landslide covering the

J., Fripiat, F., Elskens, M., Mangion, P., Chirurgien, L., Closset, I., & ... Dehairs, F. (2015). Production regime and associated N cycling in the vicinity of Kerguelen Island, Southern Ocean. Biogeosciences, 12(21), 6515.

The off-shore marine environment changes intensively with the change in the ocean depth. There are three distinctive zones that can be classified along the depth which is the Epipelagic which extends from the sea surface to a depth of 200 meters, the mesopelagic which extends from a depth of 200 meters to a depth of a 1000 meters and then the Deep sea which extends from a depth of a 1000 meters to the sea floor (Castro & Huber, 2010). The Deep sea can then be divided into a further three zones (Figure 01) Bathypelagic which extends from a depth of a 1000 meters to 4000 meters, Abyssopelagic which extends from a depth of 4000 meters to 6000 meters and then the Hadopelagic which extends which extends from a depth of 6000 meters to the sea floor (Castro & Huber, 2010).

microscopic shelled animals that have been buried deep in ocean sediment since the end of the

Submarine volcanoes, mid-ocean ridges, and submarine canyons are all grouped into the marine geology systems. Underwater structures can actually be pretty useful to marine geologists, in 1930 studies found the seafloor to have all of the same physical features on land like mountains, volcanoes, canyons and more. The seafloor is estimated to be less than 2,000,000 year old, being a lot younger than landforms. The ‘age’ difference of the two makes marine geologists’ work a lot more fun to compare in finding the way rocks are built, how the sediments are compatible and finding an estimated location of natural disasters underwater.

By testing sediment and recording whether it was deposited under conditions of normal polarity and then measuring successive layers, we can build a time chart. By matching different charts from different areas with similar fossils, a more global correlation can be made.