 I am here. So hi everyone, I just would welcome to our presentation and we'll go through some of the geochemistry that our geochemistry analysis we did for a lost or empty scores. So a simple introduction, so geochemistry, what is the geochemistry? A simple definition, geochemistry is the using of analytical chemistry for geological or archaeological purpose. What we use here, there's a number of analytical methods that can be used. It depends on what you are looking for. So if you are looking for organic matter or an organic elemental composition. During this presentation, we're going to show you two case studies. Case one is score 19, the one in the photo. We're going to go through the chemistry of score 19, then how we linked these results together and to show the final reconstruction of score 19. The case study B is mainly score 1A, and in this case study only Alice is going to show you his excellent work, how he linked the density with the systemic data. Can we move to the next slide? So the analytical method that I use are two thermal analysis and libids analysis. For the thermal analysis, I use the thermographic analyzer. And the idea behind that is to calculate the percentage of organic material and carbonate through the core. The idea is simple is just to heat the sample as certain temperature, then you use the weight of the sample before and after heating to calculate these percentages. Why is that important is to distinguish between different internalization and different layers through the core. Libids analysis, a definition of libids, libids are the organic component that does not dissolve in water but they do in chemical solvents. For this, we use gas chromatography mass spectroscopy machine. It's a separation identification machine. It's a powerful machine. We can use it for separate the component and then identify them. Before we run the sample, they need to be prepared. So basically, we extract the libids by using mix between dichrolemethane and methanol. For this process, what we are looking for, we are looking for a specific component, our specific organic compounds known as biomarkers. These are a long-lived component that can be used to distinguish between different vegetation, aquatic vegetation or terrestrial vegetation. Next slide, please. So the example of the biomarkers that I used. The first one is normal alkene. As you see in the structure is just carbon and atoms. We're going to go in details in normal alkene in the next slide. Then we have ceteroles and fatty acid. Ceteroles are a complex compound that but they produce in different structure terrestrial vegetation and aquatic vegetation. While fatty acid, they usually the high number of carbon atoms via fatty acid found in terrestrial vegetation, while the low number of carbon fatty acid low found in the aquatic vegetation. Next, please. So the normal alkene. So the normal alkene is how we distinguish between different normal alkenes that found in these samples. So the carbon alkenes that has carbon atoms from 14 to 20 usually related to bacteria and algae, while the normal alkene with c21 and c25 are found in the aquatic vegetation, as you see in the first figure, while the one with carbon atoms from 27 to 31 found in the terrestrial vegetation, which is in figure two. However, some not some mostly of the samples they they are complex ones where you found the normal alkenes from 19 to 31. Here when we are we apply a proxy known as carbon preference index where we use the big areas to apply the equation that you see. Usually the terrestrial vegetation they give carbon preference index higher than four, while the marine vegetation gives carbon preference index lower than four. Next, please. So the results. So the result of the two methods that I I I just went through are are integrated here. So the organic percentage as you see showing that in the middle of the core there is a high increasing on the growth of increasing in the percentage of organic material. Also, there is one sample in carbonate and carbonate percentage that increase increased, which may indicate that there is different kinds of soil deposit in the middle of the core. So the final analysis, we could say that the first part of of core 19 marine vegetation are are dominated in in in the first core, while terrestrial vegetation dominated the middle of the middle of the core. However, there is also some samples they give marine vegetation to the end of the core is a merged aquatic vegetation. Those what the merged plants are those usually found in lake or rivers. So this is the end of my of my part and let's move to Alex. Thank you very much, Muhammad. I'm going to take you through how we've used some x-ray fluorescence, so elemental data to help interpret the core. This data was collected on an eye track scanning XRF at Aberystwyth University. Approximately three meters of core was continuously analyzed to submit millimeter resolution. And this is important because this data set gives us a complete scan of the core. So we're not spot sampling up the core, we have a complete log so we can really start to put our finger on when events happen. Data gives us elemental abundances for about 21 elements. So at this very high resolution scanning, that's over a million data per core. It's a lot of data to play with. And we use this data to create chemical donations, a chemo stratigraphy to correlate between cores of possible and also help identify depositioned environments. We also get other data like continent rally scattering data off the core, which we can use to calculate relative densities and again help to link to seismic which I'll come to at the end of this talk. So I say we've got over a million data for year left 19. It's hard work to you know, how can we use it? What does it mean? And the way we do is a principal components analysis that's come on earlier in this conference. So what this does is takes all the different dimensions between these elements and depths and works out the main changes of it. So we've got component one along the bottom here and what you can see is that's really sulfur pulling it out along this axis as opposed to all these other elements. Component two is splitting up between these detritol minerals, silica, zirconium, rubidium, potassium, and titanium from more carbonate and organic driven elements like calcium, strontium, chlorine and bromine. But we want to get into a bit more detail. Let's say most of the variations coming on with the sulfur, this organic peak here. So we can look in our third and second and third principal components. This is our second major change in the data in the third. And this has really stuck and pulled out what's going on in the elemental data. We have rubidium, potassium, and titanium. So these elements are generally associated with different types of clay, our rillites, our smectites, our chlorites. We have bromine normally relating to salinity, strontium, calcium, and chlorine with our carbonate minerals, zirconium and silica and detritol zirconium quartz, our high energy deposition minerals, and sulfur in our organic material. So these are what we normally when we're doing chemostrictively expect elements to be associated with. And so what we can do is start to produce logs down each course. This is a three meters of core. This is silica over rubidium plotted up. So quartz over clay minerals. So as you go this way, you get higher energy deposits, this way lower energy deposits. So your sands will be up here, silks, and clays. This is all relative though. So, you know, we've got to be a bit careful as driving these names. We have carbonate over rubidium. So calcium over rubidium, which is our carbonate over clay proxy. Again, as you come this way, you get an increase in carbonate. And you can see this big spike in carbonate in the middle of the core. Sulfur rubidium is our organic proxy, again, increasing nicely and then dropping off down core. And bromine titanium is actually one of the ratio I've not used before, but came up in this study and I found it in the literature. We think it's a salinity index within wetlands. So we can see it's moderate hit spikes up here going to come on to the way we're not really going to consider that spike and then drops off at the bottom of the core. One thing I've shown some elements sediments are complex materials I've got different minerals in. And I've said look silica is in the courts, but we know the silica in every alumino silica. So it's in place as well. So how can we be sure that what I've told you is actually true and what I've got here is true? Luckily within the ALF study, we've got all sorts of other proxies to look at. So this is just core logging data down the core. So we've got different groups, medium sand, fine sand, sand down to the silts here. And what I've done is I've averaged these elemental data up for each of these observed data. And what you can see is in the sands and the silts, we've got higher levels of silica and zirconium are coarsed at minerals. Whereas in the finer sands and the silts and the clays, we've got higher levels of rubidium and potassium. So our clay minerals. So this has given confidence that what we're doing is correct. We've also got Mohammed's excellent data set. And what I've done here is plotted his organic data up against our organic proxy. And what you can see is this beautiful fit between data sets, giving us extreme confidence in this data. The same is true with our carbonate proxy and Mohammed's carbonate data. You can see that because one big spike in carbonate is coming on really nicely with our carbonate proxy as well. So from this, we've actually, we can produce a chemo stratigraphy. And this is split into six chemo units going down the core, one at the top. So chemo unit one is it made up of interbedded silts and clays with moderate wet and salinity. Chemo unit two is dropping off into a clay rich unit with decreasing organic material going down core and slightly higher saline conditions. We've then got a very sharp rows of break before we get into our unit C3, which is made of a lot of sandy carbonate material with organic material in there. This then drops off some sandy low carbonate material with decreasing organics, a clay rich silty unit of moderate organic material and low salinity and then a silty unit with very little organic and very low saline conditions. This is interpreted from the chemistry. Again, working in ELF, as you've seen, we have all sorts of other data. So I'm going to piggyback with all the talks you've seen today to show the use of chemistry. Again, just going through our main zones, moderately saline, sandy and then fresh water at the bottom. We have Mohammed's CPI data showing terrestrial biomarkers coming in in the center of the core. We have his lipid analysis and what you can see here is we're going from marine through to terrestrial organic material coming in where we're seeing our sands coming in through to this aquatic, so lacustrine fluvial material coming in with our low salinities. We've got Tom's diatom data again going from marine to fresh water over this break. We have the ecological data. So this is the rapid assessment work that Martin's talked about earlier from John. And again, these the ostracods and the fossils are showing us changing from marine through to fresh water, through to terrestrial through to fresh water deposition. Finally, as of yesterday, I've got Sam's Magsus data, which you've just seen again for this core. And again, you've seen it's dropping down at this point here where we're seeing our sands coming in before increasing at the bottom. So all these different data sets are chemistry or the organic material, the diatoms and ecological data all suggest we're going from marine to a terrestrial organic deposition environment to a fresh water environment. So again, this is just the organic material I'm talking about as terrestrial could well be a riverine environment. All these proxies agree really nicely with each other. It's great to see. Interestingly, we've got this little spike in the Magsus, which is occurring on this spike in the CPI and these little spikes in the chemistry. I only saw this yesterday. No idea what this means, but it's something we're going to look at in the future. There's also all the geocrinology that TIPM has taken you through today. We've got the OSL dates coming at about 5,000 to 6,000 years, and then the carbon 14 coming out to 9,000 to 10,000 years here. There's a break in ages here. So potentially, we've got a 3,000 million year-old conformity occurring on this sharp change in our grain size. Sharp changes in grain size normally mean an arose of surface. So again, more data agreeing with each other. So using all these data sets coming up with an integrated interpretation, at the top of our core, we have unit C1, esterine mudflats containing interbed silts and sands, low to moderate salinity, moderate organic material comprising marine vegetation of about 5,000 to 6,000 years of age. Unit C2, esterine mudflats, clay-rich material, so changing the detrital material, moderately saline again with organic material comprising marine vegetation. We have our own conformity. We then have a freshwater channel deposit comprising sand-rich carbonate material with terrestrial organic material coming in, quite large levels of organic material. Dropping down into a river or possibly lake deposit comprising a sandy layer, decreasing terrestrial organic material with depth, you can see that dropping down there. Then dropping into our lower two levels, I think that's probably the custrine due to it being clay-rich and low depositional energies comprising these finer silts or clays, terrestrial organic material. And then our bottom zone, C6, again, the custrine or potentially river or fluvial, comprising silty material, slightly sandy, you can see we've got slightly more sandy there, some interbeds in there, low levels of organic material and what it is, it's very little salinity with this emergent organic material. We can also though move into, that's analysing a single core and we want to get out from a single core into the surrounding area. So we're moving back to ELF1A, which has been talked about. Here is the Storega tsunami deposit. Here's increased amounts of both strontium, which is a shell material, and sand from the high energy deposit. And luckily for me, it's been, the seismic's been published again in this paper, Gaffnitol, and Simon's provided me with another line coming through it. And you can see there's a rose of unconformity in the base of the tsunami deposit cutting the core. This is our density curve, we've calculated from our Compton and Raleigh scattering data. And what you can see at this point here, we've got this big shift in density at the base of the core. But we've also got other smaller changes in density occurring throughout the core, coinciding with changes in the material within it. And this is important because you change the density, you change the sonic velocity of material through the core, so you get an acoustic impedance, you get a seismic reflector. And so this is just a cartoon to illustrate this, this is something I've mocked up, it's not been done by the seismic guys that might well hold their hand, you know, head in their hands when they see it. But what we've got is our big change in here coinciding with this in rose of unconformity. We have our other units that correspond really nicely with other reflectors within the package. So we can get away from a single cause worth of data and start to extrapolate out along the seismic line what we're seeing. And what we think at the top here, here's our C2 sands that I've just colored in there. We then have our C3 and our C4 chemical sands in here, these are silts and sands forming this area, are really quite small, actual tsunami deposit, underlined by clays and silts, and finally underlined by clays and interbeds. So by doing this, we've analyzed one tiny strip of about six inches through this bed that the seismic has enabled us to expand outside of it. So to conclude, it's been a whistle stop tour of it, but I've hopefully shown you how geochemical techniques are both powerful and flexible too for archaeological and paleo environmental analysis. We've shown over one million of geochemical data of different types of elemental, of lipid, of biomarkers and thermal data. And we've shown how these different geochemical data and other data agree, complement and build on each other. So that's elemental, the thermal, the biomarker, the geochronological, the ecological, and finally the magnetic susceptibility. They all agree really nicely in this call. We've shown how you can build these data up, produce a chemistotigraphy, identify chemical fashies, and then help identify the deposition environment of core ELF-19. Then switching over to core 1A, we've shown how we can use this geochemical data to directly tie it in with the seismic, help the understanding of what's causing the seismic reflectors and using these reflectors to identify sediment compositions away from the core interval. So many thanks for listening and many thanks to the team for getting me in. It's been great. Thank you very much, Alex, and Mohamed, together. Sue, if we have any questions from the attendees, please do write into the chat panel now. Everyone's wanting a cup of coffee. We are fighting a tea break, that's right. Personally, I've had that much tea and red bull today that I'm in danger of exploding if I take any more. Okay, so Richard asks, Richard Bates, how can the geochemistry be used for provenance analysis? That's something we do a lot of in our day-to-day job, so it's used throughout the oil industry and quarrying industry, all sorts of natural resources. And elements like, I've talked about zirconium, that's locked into the trital zircon, which we can use for provenance. Elements like titanium in other heavy minerals, like rutile. And the mineralogy of this material will change depending on what you're eroding into a system. So say if you're eroding a mafic body, it's going to have high levels of rutile, where if you're eroding in a felsic body, it'll have higher zirconium. So it can give us some ideas from that. But we can also actually analyze these materials themselves so we can carry out other analysis, such as heavy mineral analysis, or the trital zircon, uranium-ledge geochronology. So we can actually date these minerals so we can identify the age of the hint of land, the age of the unit, the shedding material, and also its composition. So from the chemistry we can get some idea, and then from this other techniques we can get increased ideas and really can pull apart the provenance of the area. That's great.